Geology and Paleontology of Five Cores from Screven and Burke Counties, Eastern Georgia

Home , Coryloides, Horowitz (crater), Santee Limestone

U.S. Department of the Interior U.S. Geological Survey

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

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Geology and Paleontology of Five Cores from Screven and Burke Counties, Eastern Georgia

Edited by Lucy E. Edwards

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

A description of the Cretaceous and Tertiary geology and paleontology of five cores of sediments below the coastal plain in Screven and Burke Counties, Georgia. Chapters A-l are issued as a single volume and are not available separately. U.S. DEPARTMENT OF THE INTERIOR BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY CHARLES G. GROAT, Director

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 2001

Published in the Eastern Region, Reston, Va. Manuscript approved for publication September 13,1999.

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Library of Congress Cataloging in Publication Data Edwards, Lucy E. Geology and paleontology of five cores from Screven and Burke Counties, eastern Georgia / edited by Lucy E. Edwards p. cm.—(U.S. Geological Survey professional paper; 1603) "Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey." Includes bibliographical references. 1. Geology, Stratigraphic—Cretaceous. 2. Geology, Stratigraphic—Tertiary. 3. Paleontology—Cretaceous. 4. Paleontology—Tertiary. 5. Geology—Georgia—Screven County. 6. Geology—Georgia—Burke County. 7. Paleontology—Georgia—Screven County. 8. Paleontology—Georgia—Burke County. I. Edwards, Lucy E. II. United States, Dept. of Energy. III. Georgia Geologic Survey. IV. Series. QE688.G46 2000 57.58'695—dc21 99-052940 VOLUME CONTENTS [Letters designate the chapters]

A. Stratigraphy and Depositional Environments of Sediments from Five Cores from Screven and Burke Counties, Georgia By W. Fred Falls and David C. Prowell

B. Overview of the Biostratigraphy and Paleoecology of Sediments from Five Cores from Screven and Burke Counties, Georgia By Lucy E. Edwards, Norman O. Frederiksen, Laurel M. Bybell, Thomas G. Gibson, Gregory S. Gohn, David Bukry, Jean M. Self-Trail, and Ronald J. Litwin

C. Palynomorph Biostratigraphy and Paleoecology of Upper Cretaceous Sediments from Four Cores from Screven and Burke Counties, Georgia By Norman O. Frederiksen, Lucy E. Edwards, and Ronald J. Litwin

D. Late Campanian (Zone CC 22) Coccoliths from the Millhaven Core, Screven County, Georgia By David Bukry

E. Ostracode Biostratigraphy of Upper Campanian (Cretaceous) Marine Sediments from the Millhaven Core, Screven County, Georgia By Gregory S. Gohn

F. Calcareous Nannofossil Biostratigraphy of Cenozoic Sediments from the Millhaven Core, Screven County, Georgia By Laurel M. Bybell

G. Dinocyst Biostratigraphy of Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia By Lucy E. Edwards

H. Pollen Biostratigraphy of Lower Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia By Norman O. Frederiksen

I. Foraminifera from Paleogene Sediments from the Millhaven and Millers Pond Cores, Screven and Burke Counties, Georgia By Thomas G. Gibson

in CONVERSION FACTORS

Various units used in chapters A-I are listed in the first column below.

Multiply By To obtain

Length micrometer (urn) 0.00003937 inch millimeter (mm) 0.03937 inch centimeter (cm) 0.3937 inch

inch (in.) 2.54 centimeter foot (ft) 0.3048 meter mile (mi) 1.609 kilometer

Mass ______gram (g)______0.03527______ounce avoirdupois

Sea level.—In this report, "sea level" refers to the National Geodetic Vertical Datum of 1929 (NGVD of 1929)—a geodetic datum derived from a general adjustment of the first-order level nets of both the United States and Canada, formerly called Sea-Level Datum of 1929.

IV U.S. Department of the Interior U.S. Geological Survey

Stratigraphy and Depositional Environments of Sediments from Five Cores from Screven and Burke Counties, Georgia By W. Fred Falls and David C. Prowell

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-A

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract ...... Al Introduction ...... 1 Test Hole and Core Information ...... 2 Previous Work ...... 4 Acknowledgments ...... 4 Stratigraphic Framework...... 4 Cretaceous Stratigraphy ...... 7 Cape Fear Formation ...... 9 Middendorf Formation ...... 10 Black Creek Group ...... 10 Steel Creek Formation ...... 11 Tertiary Stratigraphy ...... 12 Ellenton Formation ...... 12 Snapp Formation ...... 13 Fourmile Branch/Congaree/Warley Hill Unit ...... 13 Santee Limestone ...... 14 BarnwellUnit ...... 16 Summary ...... 17 References Cited ...... 17

FIGURES

1. Index map showing the Savannah River Site and the location of Stratigraphic test holes in the study area ...... A2 2. Correlation diagram showing a generalized comparison of Cretaceous and Tertiary geologic units in the Southeastern United States...... 3 3-5. Gamma-ray, single-point resistance, and lithologic logs and geologic units of the•— 3. Millhaven test hole in Screven County, Ga...... 5 4. Girard test hole in Burke County, Ga...... 6 5. Millers Pond test well 1 and test hole in Burke County, Ga...... 7 6. Gamma-ray, single-point resistance, and lithologic logs (from figs. 3-5) showing dip-oriented correlation of geologic units from the Millers Pond test hole to the Millhaven test hole ...... 8

TABLE

Iilevations and depths of Stratigraphic tops for geologic units and subunits in the Millhaven, Girard, Thompson Oak, Millers Pond, and McBean cores...... A9

III

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Stratigraphy and Depositional Environments of Sediments from Five Cores from Screven and Burke Counties, Georgia

By W. Fred Falls and David C. Prowell

ABSTRACT the Snapp Formation, generally is more calcareous and has a more diverse and abundant marine microflora and fauna in Five deep stratigraphic test holes were drilled from the downdip Millhaven core, relative to the updip McBean 1991 to 1993 in support of multidisciplinary investigations and Millers Pond cores. For these units, sedimentary and to determine the stratigraphy of Upper Cretaceous and Ter paleontologic evidence suggests open-marine shelf environ tiary sediments of the coastal plain in east-central Georgia. ments at the Millhaven site and marginal-marine environ Cored sediment and geophysical logs from the Millhaven ments at the Millers Pond site. test hole in Screven County and the Girard and Millers Pond The Snapp Formation is nearly barren of fossils and is test holes in Burke County are the primary sources of litho- a noncalcareous sequence of oxidized sand and clay. Sedi logic and paleontologic information for this report. Litho- mentary characteristics of the Snapp Formation suggest a logic and paleontologic information from the Thompson fluvially dominated depositional environment such as an Oak and McBean test holes in Burke County supplements upper delta plain or an incised alluvial valley. The presence the discussion of stratigraphy and sedimentation in the of a sparse marine microflora suggests some marine influ updip part of the study area near the Millers Pond test hole. ence on deposition in the downdip area near Millhaven. Dif The Cretaceous sections in the studied cores are ferences in the thickness of this formation in the study area divided into the Cape Fear Formation, the Middendorf For suggest that channels containing the basal sand of the Snapp mation, the Black Creek Group, and the Steel Creek Forma Formation are incised into laminated black clay of the tion. These four geologic units consist of siliciclastic Ellenton Formation. sediments. Evidence of possible unconformities allows us to recognize two subunits in the Middendorf Formation and three subunits in the Black Creek Group. Sediments in the Cretaceous section generally are coarser grained and more INTRODUCTION oxidized in updip areas. Each contact between units is a regional unconformity and denotes a considerable hiatus in Five deep stratigraphic test holes were drilled in sedimentation. The sediments in all four geologic units have east-central Georgia from 1991 to 1993 in support of multi- been interpreted as being part of large deltaic systems that disciplinary investigations by the U.S. Geological Survey prograded across the paleo-continental shelf in east-central (USGS) and the Georgia Geologic Survey (GGS) of the Georgia and western South Carolina. The lithofacies Georgia Department of Natural Resources. These investiga observed in the Upper Cretaceous units tend to be coarser tions were conducted to determine the geology and hydrol grained in proximal-deltaic environments and finer grained ogy of the Georgia Coastal Plain sediments in the vicinity of in distal-deltaic environments. the U.S. Department of Energy Savannah River Site (SRS) The Tertiary sections are divided into the Ellenton and in South Carolina (fig. 1). In this region, poorly consoli Snapp Formations of Paleocene age; the Fourmile Branch/ dated Cretaceous and Cenozoic strata form a southeast Congaree/Warley Hill unit and Santee Limestone of Eocene ward-thickening wedge of fluvial and marine deposits age; and the Barn well unit, which contains strata of Eocene underlain by Paleozoic crystalline rocks and Triassic-Juras- to Miocene age. The Tertiary section, with the exception of sic sedimentary rocks. This wedge of sediment is more than

Al A2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

8230 82 8130 TEST HOLE AND CORE INFORMATION

The five test holes informally are named for local land marks and formally are assigned either a GGS or a USGS identification number. The informal names used in this report are Millhaven, Girard, Thompson Oak, Millers Pond, 33° 30 and McBean. The five test holes were continuously cored with a wireline, mud-rotary coring system. The cores from the Millhaven, Girard, and Millers Pond test holes were examined for texture, mineralogy, sedimentary structures, diagenetic features, and the presence of macrofossils. Selected samples were examined microscopically for 33° dinoflagellates, pollen, foraminifers, ostracodes, and calcar eous nannofossils. The descriptions of the cores and the geophysical logs of the associated test holes at Millhaven, Girard, and Millers Pond are the primary sources of infor mation for the following discussion of stratigraphic units (Clarke and others, 1994, 1996; Leeth and others, 1996). 32°30'- The authors interpreted the stratigraphy of the Thomp son Oak and McBean cores from descriptions published by the GGS (Huddlestun and Summerour, 1996) and have not

Test hole site and informal name of site personally examined these cores in detail. Samples for paleontologic examination were collected by PF. Huddlestun of the GGS from the Thompson Oak and McBean cores. We Figure 1. Index map showing the Savannah River Site and the used the paleontologic results (Frederiksen and others, this location of stratigraphic test holes in the study area. volume, chap. C; Edwards, this volume, chap. G; Frederik sen, this volume, chap. H) to interpret the stratigraphy and sedimentation of geologic units in the updip area near Mill 1,450 ft thick in the downdip Millhaven core in Screven ers Pond in Burke County, Ga. The stratigraphies of these County. two cores supplement the following discussion of stratigra phy in the updip part of Burke County near the Millers Pond Previously, the Upper Cretaceous section in the sub test hole but are not illustrated as stratigraphic columns in surface of the study area was penetrated partially by four this report. cored test holes along the Savannah River in Burke County (Bechtel Corporation, 1972) and by a cored test hole near Geophysical-logging surveys of the test holes, with the the town of Midville in the southwestern corner of Burke exception of the McBean test hole, include single-point and County (Prowell, Christopher, and others, 1985). The Creta triple-point electric resistance, spontaneous potential, natu ceous section also was studied by using geophysical logs ral gamma ray, and hole diameter (caliper log). Formation and cuttings from local water wells (Clarke and others, instability and hole diameter of the Millhaven test hole pre 1985). The sedimentary history and stratigraphy of the Ter vented electric-logging surveys of the section from 571 to tiary section in the study area already were known from out 530 ft and triple-point resistance logging below 900 ft. The crops (Huddlestun and Hetrick, 1978, 1979, 1986; Hetrick, McBean test hole is the only one studied that was not geo- 1992) and from several fully or partially cored test holes in physically logged. northern Burke County (McClelland, 1987) and along the Savannah River in Burke and Screven Counties (Bechtel Figure 2. Generalized comparison of Cretaceous and >- Corporation, 1972). Tertiary geologic units in the Southeastern United States This chapter briefly describes the lithologic and strati- (modified from Clarke and others, 1994). Shaded areas indicate graphic character of the geologic units (fig. 2) recognized in missing stratigraphic sections. Dashed lines indicate formation the five cored sections to provide a framework for detailed boundary of uncertain stratigraphic position. Abbreviation used: Fm, formation. Source for the lithologic units of eastern discussions of the fauna and flora identified from paleonto Georgia: Prowell, Christopher, and others (1985). Sources for logic efforts. The paleontologic data presented in the other the Georgia Geologic Survey nomenclature in eastern Georgia: chapters of this volume are used with the core descriptions Huddlestun and Hetrick (1991), Summerour and others (1994), to infer correlation of these geologic units with stratigraphi- and Huddlestun and Summerour (1996). Sources for units of cally equivalent units in the vicinity of the study area and to South Carolina: Colquhoun and others (1983), Gohn (1992), infer depositional environments. and Fallaw and Price (1995). SERIES EUROPEAN PROVINCIAL WESTERN EASTERN GEORGIA SOUTH Lithologic Georgia Geologic THIS STUDY subseries ALABAMA STAGE STAGE GEORGIA unit Survey Nomenclature EASTERN GEORGIA CAROLINA Miocene Hawthorn Formation Undifferentiated Undifferentiated Mi Hawthorn Formation

""---:-... Edisto Formation CD Paynes Hammock Sand Chandler Bridge Format on c CD Chickasawhayan Suwannee Limestone O Chattian Chickasawhay Formation Cooper Formation (Ashley Member) O 01 CT Byram Formation Barnwell Vicksburgian Marianna Formation O Rupelian Red Bluff Clav/Bumpnose Fm. unit / Ocala CL \ Parkers Ferry 05 E8 e Tobaccc Q. Ocala 5 \ Harleyville Fms. Q. Priabonian Barnwell = RoadSarid/ (Cooper Group) =) Jacksonian Limestone Clay ^_^ E7 Group | Dry Bran *v ™ Clinchfie Moodys Branch Fm. Moodys Branch Fm. E6 CD Bartonian A—— Gosport Sand 05 Santee Tinker CL § "O ) Santee Lisbon Formation O O T3 E5 Limestone Formation LLJ Lisbon Formation Lisbon Formation _/ Formation CD Lutetian E4 Still Branch Sand Warley Hill Fm.\ Claibornian Fourmile Branch/ OJ Tallahatta Tallahatta E3 Congaree/ Huber / Congaree \ O5 Congaree 1 Formation Formation Fm. y Formation / O E2 Formation Warley Hill unit 1 Ypresian O Hatchetigbee/Bashi Fms. Hatchetigbee/Bashi Fms. E1 Fourmile Branch Fm.^[snburne Fm- Thanetian Sabinian Tuscahoma Formation Tuscahoma Formation finapp Formation / 05 Nanafalia/Baker Hill Fms. Nanafalia/Baker Hill Fms. Snapp Formation i /Williamsburg BlackMingoGroup Q. Lang Syne Paleocene Q. / \ Formation =3 'Jaheola Fm.>- Formation / Selandian Black Mingo Ellenton —————— (Ellenton /———— Porters Creek Porters Creek Formation P1 Midwayan Formation Formation Sawdust \v Fm- ( Rhems Landing Fm. Danian Clayton Formation Clayton Formation (Undifferentiated) ; J Fm. 1

Prairie Bluff Chalk Maastrichtian Providence Sand UK6 Steel Creek Steel Creek / Peedee Navarroan Ripley Formation Formation / Formation Ripley Formation Steel Creek Fm. Formation Donoho Creek Fm. Black Creek Black Demopolis Chalk Bladen Formation Cusseta Sand UK4 Gaillard / Black Group Creek Tayloran Group Coachman Formation CO Campanian Fm. ( Creek Cane Acre Formation \ Fm. O Caddin Formation CD Mooreville Chalk Blufftown Formation UK3 O Shepherd Grove Fm. CO Middendorf Formation Austinian Eutaw Formation Pio Nono> Unnamed Santonian Eutaw Formation UK2 Middendorf Formation CD Fm. > Sand O Coniacian McShan Formation Tuscaloosa Formation UK1 Cape Fear Formation Cape Fear Formation __ „ ™. „..„. „ __ „. _ „, m .„.. „. __ _ m _ CD Q. Turanian : ! : Q. ---...... ID Eaglefordian Tuscaloosa Formation Tuscaloosa Formation Cape Fear Clubhouse Formation Formation Cenomanian /Woodbinian x Beech Hill Washitan (part) Formation A4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

The Millhaven test hole was drilled by the USGS in PREVIOUS WORK late 1991 and early 1992 and formally designated as 33X048 (Clarke and others, 1996). The Millhaven site is Previous reports on the geology of Burke and Screven located in Screven County, Ga., at lat 32°53'25" N., long Counties and adjacent areas of Georgia include those by 81°35'43" W. (fig. 1) and has a land surface elevation of 110 Veatch and Stephenson (1911), Brantley (1916), Cooke and ft. The test hole was drilled from land surface to a total Shearer (1918), Cooke (1943), LaMoreaux (1946a,b), depth of 1,452 ft (fig. 3). This test hole was terminated in LeGrand and Furcon (1956), Herrick (1960, 1961, 1964, Upper Cretaceous sediments of the Cape Fear Formation 1972), Herrick and Vorhis (1963), Herrick and Counts and did not reach pre-Cretaceous rocks. (1968), Bechtel Corporation (1972, 1973), Carver (1972), Buie (1978), Huddlestun and Hetrick (1978, 1979, 1986, The USGS drilled the Girard test hole in the spring of 1991), Prowell and O'Connors (1978), Schroder (1982), 1992 and formally designated it as 32Y020 (Leeth and oth McClelland (1987), Huddlestun (1988, 1992), Hetrick ers, 1996). The Girard site is in Burke County, Ga., at lat (1992), Clarke and others (1994, 1996), Huddlestun and 33°03'54" N., long 81°43'13" W. (fig. 1) and has a land sur Summerour (1996), Leeth and Nagle (1996), Leeth and face elevation of 250 ft. The test hole was drilled from land others (1996), and Falls and others (1997). Geologic reports surface to a total depth of 1,385 ft and penetrated 1,375 ft of on Burke and Screven Counties and adjacent parts of South coastal plain sediments (fig. 4) and 10 ft of continental red Carolina include those by Snipes (1965); Hurst and others beds of probable Triassic or Jurassic age (Siple, 1967; (1966); Scrudato and Bond (1972); Daniels (1974); Marine Marine, 1979; Prowell, Christopher, and others, 1985). and Siple (1974); Bechtel Corporation (1982); Faye and Prowell (1982); Huddlestun (1982); Prowell, Christopher, The GGS drilled the Thompson Oak test hole in early and others (1985); Colquhoun (1991, 1992); Edwards 1993 and formally designated it as GGS-3794 (Summerour (1992); Fallaw and Price (1992, 1995); Harris and Zullo and others, 1994; Huddlestun and Summerour, 1996); it is (1992); and Prowell (1994). Geologic reports on adjacent also known as TR92-6 and Burke 12. The drill site is parts of South Carolina include those by Sloan (1908); located in Burke County, Ga., at lat 33°10'42" N., long Cooke (1936); Cooke and MacNeil (1952); Christl (1964); 81°47'10" W. (fig. 1) and has a land surface elevation of 240 Siple (1967); Marine (1979); Smith (1979); Nystrom and ft. The test hole was drilled from land surface to a total Willoughby (1982); Zullo and others (1982); Colquhoun depth of 1,010.5 ft and penetrated 996 ft of coastal plain and others (1983); Bledsoe (1984, 1987, 1988); Colquhoun sediments and 14.5 ft of biotite gneiss of probable Paleozoic and Steele (1985); Steele (1985); Prowell, Edwards, and age. Frederiksen (1985); Nystrom and others (1986, 1991); The GGS drilled the Millers Pond test hole, also Dennehy and others (1989); Logan and Euler (1989); known as Burke 2, in the summer of 1991 and formally des Robertson (1990); Colquhoun and Muthig (1991); Price and ignated it as GGS-3758 (Clarke and others, 1994). The site others (1991); Fallaw and others (1992a,b); Snipes and is located in Burke County, Ga., at lat 33°13'48" N., long others (1993); and Gellici and others (1995). 81°52'44" W. (fig. 1) and has a land surface elevation of 245 ft. The test hole was drilled from land surface to a total depth of 859 ft and penetrated 852 ft of coastal plain sedi ACKNOWLEDGMENTS ment (fig. 5) and 7 ft of biotite-hornblende gneiss of proba The authors thank the U.S. Department of Energy for ble Paleozoic age. A nearby hole, Millers Pond test well 1, its support of this investigation. They also thank the Georgia was logged for geophysical properties. Geologic Survey for allowing access to the Millers Pond The GGS drilled the McBean test hole, also known as core, and Paul F. Huddlestun for sampling and providing Burke 5, in 1991 and formally designated it as GGS-3757 lithologic descriptions of the Thompson Oak and McBean (Summerour and others, 1994; Huddlestun and Summerour, cores. The authors also acknowledge the efforts of Donald 1996). The drill site is near the community of McBean in G. Queen, Eugene F. Cobbs, and Gerald E. Idler during the Burke County, Ga., at lat 33°13'38" N., long 81°55'50" W. coring and logging of the Millhaven and Girard sites. (fig. 1) and has a land surface elevation of 297 ft. The test hole was drilled from land surface to a total depth of 327 ft and terminated in the upper part of the Upper Cretaceous STRATIGRAPHIC FRAMEWORK section. Lithologic data from the Millhaven, Girard, and Mill Stratigraphic tops, stratigraphic details, and samples ers Pond cores and geophysical logs from the three associ for paleontologic analysis in this volume are reported as ated test holes were used to define the four Cretaceous and core depth below land surface. Geophysical logs for the five Tertiary units in this study (fig. 2). Correlation of these Millhaven, Girard, and Millers Pond test holes were geologic units in the Millhaven, Girard, and Millers Pond adjusted slightly to match core depth. cores is presented in a dip-oriented cross section (fig. 6). STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A5

Gamma ray Single-point Geologic (API units) Lithology resistance (ohms) unit 0 150 100 200

100 - Barnwell - 100 unit

200 - - 200

300 - Santee - 300 Limestone

400 - - 400 Fourmile Branch/ Congaree/ Warley Hill 500 - unit - 500 Snapp Formation

600 - Ellenton - 600 Formation

700 - - 700

Steel Creek EXPLANATION Formation FOR FIGURES 3-5

800 - - 800 Limestone

Sandy limestone 900 - - 900

_^_^J Massive clay

1000 - Black Creek _ 1000 Laminated clay Group Sand

1100 - - 1100 lE-IJEH Clayey sand

1200 - - 1200

Middendorf Formation 1300 - - 1300

Figure 3. Gamma-ray, single-point resistance, 1400 - Cape - 1400 and lithologic logs and geologic units of the Fear Millhaven test hole in Screven County, Ga. Formation 1452 1452 Abbreviation used: API, American Petroleum Land Surface Elevation = 110 feet above sea level. Institute. A6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Gamma ray Single-point Geologic (API units) Lithology resistance (ohms) unit 0 150 100 200

100 - - 100 Barnwell unit

200 - - 200

300 - - 300 Fourmile Branch/ Congaree/ 400 - Warley Hill - 400 unit

Snapp Formation - 500 500 - Ellenton Formation

Steel Creek 600 - Formation - 600

700 - - 700

Black Creek 800 - Group - 800

900 - - 900

1000 - - 1000

Middendorf Formation 1100 - - 1100

1200 - - 1200

Cape Fear Figure 4. Gamma-ray, single-point resis Formation 1300 - - 1300 tance, and lithologic logs and geologic units of the Girard test hole in Burke County, Ga. Abbreviation used: API, American Petroleum 1375 1375 Institute. Lithologic patterns are explained in figure 3. Land Surface Elevation = 250 feet above sea level. STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A7

Gamma ray Single-point Geologic (API units) Lithology resistance (ohms) unit 0 150 175 200

Barnwell unit

100 - Santee - 100 Limestone Fourmile Branch/ Congaree/ Warley Hill unit 200 - Snapp - 200 Formation Ellenton Formation Steel Creek 300 - - 300 Formation

400 - - 400 Black Creek Group

500 - - 500

600 - - 600

Middendorf Formation 700 - - 700

Figure 5. Gamma-ray, single-point resistance, and lithologic logs and geologic units of the 800 - Cape Fear - 800 Formation Millers Pond test well 1 and test hole in Burke County, Ga. Abbreviation used: API, American 852 852 Petroleum Institute. Lithologic patterns are Land Surface Elevation = 245 feet above sea level. explained in figure 3.

The section roughly parallels the Savannah River and and nomenclature used in this report result from combining reflects the thicknesses and stratigraphy of the geologic information from these reports. units from the updip Millers Pond site to the downdip Mill- Huddlestun and Hetrick (1991), Summerour and others haven site. Datum for the section is sea level. The elevation (1994), and Huddlestun and Summerour (1996) proposed a and depth of the stratigraphic top of each geologic unit in stratigraphic nomenclature for the updip part of the study these three cores and the Thompson Oak and McBean cores area in east-central Georgia. A comparison of the strati- are listed in table 1. graphic units for previous studies with the stratigraphy in this study is shown in figure 2. The stratigraphy of the Mill- Prowell, Christopher, and others (1985) correlated haven, Girard, and Millers Pond cores is shown in figures 3, Cretaceous and Tertiary geologic units in the updip coastal 4, and 5. plain from central Georgia to western South Carolina. They identified five of the six Upper Cretaceous units, two Pale- ocene units, six of the eight Eocene units, and one Oli- CRETACEOUS STRATIGRAPHY gocene unit in a South Carolina drill hole at the SRS (fig. 2). Their units were essentially chronostratigraphic units that The Cretaceous sediments in the study area are divided were assigned alpha-numeric designations because of a lack into the Cape Fear Formation, the Middendorf Formation, of existing nomenclature. Subsequently, Fallaw and Price the Black Creek Group, and the Steel Creek Formation (fig. (1995) established a working nomenclature and described 2). These four geologic units consist of siliciclastic sedi the stratigraphic units beneath the SRS. The stratigraphy ments, are coarser grained and more oxidized in updip GIRARD 300 MILLERS POND Gamma ray Lithology Resistance Gamma ray Lithology Resistance 200 MILLHAVEN

Gamma ray L thology Resistance 100 3>- -w SEA - Onj>OOOOOOOOOOOOO3O LEVEL -'_|i-(Moo^mcDr^oooi-ooj-1-I-I--I-T--uSOOfnLLJOOOO OOOOOOi-OJCO'*

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Figure 6. Gamma-ray, single-point resistance, and lithologic logs (from figs. 3-5) showing dip-oriented correlation of geologic units from the Millers Pond test hole to the Millhaven test hole. Datum is sea level. STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A9

Table 1. Elevations and depths of stratigraphic tops for geologic units and subunits in the Millhaven, Girard, Thompson Oak, Millers Pond, and McBean cores. [The stratigraphic contacts in the Thompson Oak and the McBean cores are interpreted from lithologic descriptions provided by Paul F. Huddlestun, Georgia Geologic Survey, Atlanta, Georgia. The stratigraphic contacts and names for the Thompson Oak and McBean cores in this table represent the stratigraphic interpretations of the authors and do not agree with Huddlestun's interpretations in all cases. Elevations are in feet above or below sea level. Depths are in feet below land surface. Top of Barnwell unit equals land surface in each core. N.D., not determined; N.P., not penetrated]

Elevation/depth of stratigraphic contact Name of geologic unit Millhaven Girard Thompson Oak Millers Pond McBean core core core core core

110/0 250/0 240/0 245/0 297/0 1 1 8/998 0/250 110/130 163/82 185/112 Fourmile Branch/Congaree/ Warley Hill unit - -291/401 -75/325 58/182 89/156 111/186 Warley Hill Formation ———————— 291/401 absent absent absent absent 35^/462 75/325 58/182 89/156 111/186 absent 140/390 11/251 absent absent Snapp Formation ———————————— 394/504 173/493 absent 80/165 75/222 Ellenton Formation ———————————— -460/570 931/481 34/974 13/232 25/272 Steel Creek Formation ———————————— ^79/649 992/54'? 54/394 39/284 -8/305 790/R30 309/649 -166/406 87/799 N.P. 799/839 392/64^ 166/406 R7/399 N.P. Subunit 2 ————————————— 817/927 -482/733 N.D. N.D. N.P. 1,009/1,119 -659/909 N.D. N.D. N.P. -1,062/1,172 -708/958 -445/685 -347/592 N.P. Subunit 2 ————————————— 1,062/1,172 708/958 -445/685 347/509 N.P. Subunit 1 ————————————— 1 1 ^O /1 OT") o i o /1 r\£i^t -485/725 -418/663 N.P. Cape Fear Formation —————————— 1,269/1,379 913/1,163 -602/842 507/752 N.P. N.P. 1,125/1,375 -756/996 -603/852 N.P.

areas, and become finer grained in a coastward direction. CAPE FEAR FORMATION Unit contacts are typically overlain by lags of very poorly sorted sand containing granules, pebbles, and lithoclasts. The Cape Fear Formation consists of partially lithified Each contact is considered to be a regional unconformity to unlithified, poorly to very poorly sorted clayey sand and and probably denotes a considerable hiatus in sedimenta sandy clay with a few beds of silty clay. The sand is fine to tion. In the updip area, lithologic similarities among the very coarse with granules and pebbles and is predominantly units and the presence of only a few fossil-bearing beds angular to subangular quartz with some feldspar. Cristo- make it difficult to identify unit contacts at Millers Pond. balite in the clay matrix results in lithologies that are harder Evidence of possible unconformities is used to divide the and denser than sediments in the other Cretaceous units. Middendorf Formation into two subunits in the Millhaven, The cristobalitic clay matrix imparts a yellowish-green to Girard, and Millers Pond cores, and the Black Creek Group greenish-gray color to most of the lithologies and occludes into three subunits in the Millhaven and Girard cores. Prow- most of the intergranular porosity in the sand beds. Electric ell, Christopher, and others (1985) identified units UK1 logs display low resistance in the sands and the clays in through UK6 in their study but did not correlate their unit most of this unit. Sands in the upper 10 to 20 ft of this unit UK3 with units in the test holes at the SRS. in the Millhaven and Girard cores are unlithified and have atypically high resistance values on the electric logs. Biostratigraphic studies by Christopher (1978) and Prowell, Christopher, and others (1985) suggested that Cre The Cape Fear Formation contains multiple fining- taceous strata in east-central Georgia ranged in age from upward cycles that range in thickness from 3 to 15 ft. Each Coniacian to Maastrichtian. The sediments in the four units cycle grades upward from a basal coarse pebbly sand to have been interpreted as parts of large deltaic systems that clayey sand or clay. The clays are oxidized and are generally prograded across the paleo-continental shelf in east-central stained with reddish-brown and yellowish-brown patches of Georgia and western South Carolina (Prowell and others, iron oxide. A root-trace pattern is present at the top of a few 1985a; Fallaw and Price, 1995). Lithofacies observed in the of the fining-upward cycles and at the top of this unit in the Upper Cretaceous units accumulated in coarser grained Millhaven core. Sediments directly beneath the upper con proximal and finer grained distal deltaic settings. tact of the Cape Fear Formation in the other cores are A10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

stained with iron oxides. Lag deposits at the base of the lag deposit of poorly sorted sand that grades up to interbed- Cape Fear Formation contain clasts of saprolitic gneiss in ded and interlaminated clay and sand. Micaceous and lig- the Millers Pond core and clasts of Trias sic siltstone in the nitic sand laminae are common in the Middendorf sections, Girard core. particularly near the top of each subunit. Clay beds are gen Most of the strata in this unit are barren of fossils, but a erally thicker and display more abundant iron-oxide staining few samples of gray and olive-gray, silty clay from the Mill near the top of each subunit in the Millers Pond and Girard ers Pond core yielded low-abundance and low-diversity pol cores. A root-trace pattern is observed in the clay at the top len assemblages. Palynologic analysis of these samples of subunit 2 in the Girard core. Clays at the top of each sub- from the Millers Pond core (Frederiksen and others, this unit in the Millhaven core are not stained with iron oxides. volume, chap. C) indicates a Coniacian microflora that is Lithologic data and geophysical log patterns seem to consistent with the microflora of the Cape Fear Formation indicate that the upper contact of the Middendorf Formation of South Carolina and North Carolina (Christopher and oth in the Georgia cores correlates with the unit UK2/UK4 ers, 1979; Christopher, 1982; Sohl and Owens, 1991). Prow- boundary of Prowell, Christopher, and others (1985) and the ell, Christopher, and others (1985) and Fallaw and Price top of the Middendorf Formation as recognized by Fallaw (1995) suggested a Santonian age for unit UK1 and the and Price (1995) at the SRS. A Santonian age was reported Cape Fear Formation at the SRS. Huddle stun and Summer- for unit UK2 by Prowell, Christopher, and others (1985) and our (1996) suggested that the Cape Fear Formation is equiv for the Middendorf Formation at the SRS by Fallaw and alent to the Cenomanian-Turonian Tuscaloosa Formation of Price (1995). Samples collected at 1,138 and 1,012 ft in the western Georgia. Samples from this formation were not pro Girard core and 1,212 ft in the Millhaven core contain cessed for the other cores. pollen that suggests at least part of the Middendorf The presence of a terrestrial microflora and the Formation may be correlative with the Shepherd Grove absence of dinoflagellates and other marine fossils in the Formation, which overlies the Middendorf in South Cape Fear Formation suggest deposition in a nonmarine Carolina (Frederiksen and others, this volume, chap. C). environment at Millers Pond. The Cape Fear Formation in All or part of what has been described as Middendorf the Millhaven and Girard cores is lithologically similar to Formation in this part of Georgia may actually be correla the section in the Millers Pond core and also is interpreted tive with part of the Black Creek Group or an updip lithofa- as having been deposited in a nonmarine environment. The cies of either the Caddin or Shepherd Grove Formations, multiple fining-upward cycles, the coarse texture of the which Gohn (1992) identified as late Santonian to early sands, the iron-oxide staining, and root-trace patterns in the Campanian in age. Evidence of subaerial exposure and ero- clays suggest that most of this unit was deposited in channel sional lags at the contacts between the upper and lower sub- and overbank environments during aggradation of a flu- units support the possibility that unit UK2 (Prowell, vially dominated, subaerially exposed part of a delta-plain Christopher, and others, 1985), as defined beneath the environment. southeastern corner of the SRS, contains more than one depositional sequence and is equivalent in part to unit UK3. Huddlestun and Hetrick (1991) applied the name Pio MIDDENDORF FORMATION Nono Formation in updip areas of east-central Georgia to the Middendorf Formation as used here. Dinoflagellates and The Middendorf Formation consists predominantly of other marine indicators are sparse and suggest a mar unlithified sand, which is locally fine to very coarse or fine ginal-marine environment at Millhaven and a nonmarine to medium quartz (figs. 3, 4, 5). The sand includes environment for this unit in the other cores. smoky-quartz granules and pebbles, mica, lignite, and gen erally very little clay matrix. The Middendorf sands are moderately to poorly sorted and are very porous and perme BLACK CREEK GROUP able in comparison with the sands in the underlying Cape Fear Formation. Black clay is present in laminae and thin The Black Creek Group consists of three distinct sub- beds that are less than 2 ft thick in the Millhaven core. Clay units in the Millhaven and Girard cores: a basal lignitic sand beds in the Millers Pond core and most of the Girard core in subunit 1, a laminated black clay and sand in subunit 2, generally are light gray to white and range in thickness from and a coarsening-upward sand sequence in subunit 3 (figs. 1 to 10 ft. 3, 4, table 1). The lag deposits at the bases of the subunits The Middendorf Formation contains two distinct sub- suggest the possibility of unconformities in the Black Creek units in the Millhaven, Girard, and Millers Pond cores. Group at Millhaven and Girard. The Black Creek Group at Additional work in the study area may show these subunits Millers Pond is coarser and sandier and is not divided into to be separate, mappable formations. At present, they are subunits (fig. 5). informally referred to in ascending order as subunits 1 and 2 Black Creek subunit 1 consists of moderately to poorly of the Middendorf Formation. Each subunit includes a basal sorted, fine to coarse quartz sand that grades into overlying STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A11 very fine to fine sand with a few thin beds of clay. The sand others, this volume, chap. C; Bukry, this volume, chap. D; contains abundant interlaminated fine lignite and mica and Gohn, this volume, chap. E). Units UK4 and UK5 (Prowell, very little clay matrix. This subunit is lithologically very Christopher, and others, 1985) and the Black Creek Group similar to the underlying Middendorf Formation. at the SRS (Fallaw and Price, 1995) are assigned an age of Black Creek subunit 2 in the Millhaven core has a Campanian to Maastrichtian. Huddlestun and Hetrick sharp basal contact at 1,119 ft and a second sharp contact at (1991) applied the name Gaillard Formation to the fluvial 1,099 ft. Each contact is overlain by a basal lag deposit of lithofacies in the updip Georgia Coastal Plain. Paleontologic very poorly sorted sand. The sand above the contact at 1,099 data (Frederiksen and others, this volume, chap. C; Bukry, ft grades and fines into an overlying 161-ft section of pre this volume, chap. D; Gohn, this volume, chap. E) suggest dominantly silty laminated black clay. The 161-ft clay sec that the calcareous lithologies of subunit 2 at Millhaven are tion also includes very fine to fine sand from 1,063 to equivalent to the Donoho Creek Formation of the Black 1,051 ft. Most of subunit 2 is calcareous and contains lami Creek Group (Owens, 1989; Sohl and Owens, 1991). nae and lenses of very fine sand and sand-filled burrows. The diversity and abundance of dinoflagellates, the Very fine to fine sand is interlaminated at the top of the clay abundance of marine faunas, and the presence of glauconite from 934 to 927 ft. Subunit 2 in the Girard core is sandier at Millhaven and Girard suggest a strong marine influence and consists of very fine to fine sand with interbedded black during the deposition of subunit 2, probably in the distal clay. The sand at Millhaven and Girard includes mica, lig part of a deltaic complex. Dinoflagellates in subunit 3 sug nite, and minor amounts of glauconite. gest a marginal-marine depositional environment. The com Bioturbation features in subunit 2 at Millhaven and position of the microflora and the absence of other marine Girard include clay-lined burrows, mottled textures, and dis indicators suggest that subunit 1 at Millhaven and Girard continuous laminae of clay in the sands. Subunit 2 at Mill- and the entire section of the Black Creek Group at Millers haven and Girard yielded the most abundant and diverse Pond reflect sedimentation in a nonmarine part of the delta marine macrofaunas and microfaunas and microfloras in the (Frederiksen and others, this volume, chap. C). Cretaceous section in the study area, including shark teeth, pelecypods, ostracodes, benthic and planktonic foraminifers, spicules, dinoflagellates, pollen, and calcareous nanno- STEEL CREEK FORMATION fossils (Bukry, this volume, chap. D; Frederiksen and others, this volume, chap. C; Gohn, this volume, chap. E). Most of the Steel Creek Formation in the Georgia test Black Creek subunit 3 in the Millhaven core is a coars holes consists of poorly to very poorly sorted, fine to very ening-upward sequence and consists of a very poorly sorted coarse sand with granules and pebbles of smoky quartz and lag deposit from 927 to 926 ft; moderately to well-sorted, 5 to 15 percent clay matrix (figs. 3, 4, 5). The basal lags are very fine to medium sand from 926 to 880 ft; and moder overlain by thick intervals of oxidized clay in the Millhaven ately sorted, fine to coarse sand from 880 to 826 ft. This and Girard cores. Steel Creek sections include multiple fin subunit at Millhaven includes laminae and thin beds of ing-upward sequences with beds of coarser grained sand dark-gray clay, large and small pieces of lignite, and mica; that become finer and grade into overlying clay beds. Many the subunit is crossbedded from 907 to 900 ft. of the clay beds are stained with iron oxide and contain as Black Creek subunit 3 in the Girard core has a sharp much as 40 percent sand by volume. Root traces typically basal contact at 733 ft and a lag deposit of very poorly are present at the top of the thick oxidized clay near the base sorted sand and granules from 733 to 730 ft. The section of the section and in some of the clay beds near the top of includes beds of moderately to poorly sorted, medium to this unit. Crossbedding is common at Millhaven. Lignite very coarse sand; and moderately sorted, fine to medium and mica are common accessory constituents. sand with 5 to 10 percent clay matrix. This section is cross- Kidd (1996) used a subtle difference in grain size and bedded from 714 to 710 ft and 679 to 660 ft and includes clay content and geophysical-log correlations with test holes one light-gray, iron-stained clay from 685 to 679 ft. The top on the SRS to identify the contact between the Black Creek of the clay at 679 ft is overlain by a lag deposit of very Group and the Steel Creek Formation at 397 ft in the Millers poorly sorted sand and granules. Pond core. Huddlestun and Summerour (1996) identified The Black Creek Group at Millers Pond contains the basal contact at 367 ft in the Millers Pond core and 414 poorly sorted, fine to very coarse sand and beds of clay (fig. ft in the Thompson Oak core; they described the contact 5). Granules and pebbles are more abundant and form sev between the Black Creek (Gaillard) and Steel Creek Forma eral very poorly sorted lags at the base of sand beds, which tions as either conformable or paraconformable in updip generally include clay clasts. The sand is unlithified and has parts of Burke County and as gradational in the Girard core. minor amounts of clay matrix. The tops of clay beds gener The contact between the Black Creek Group and the Steel ally are stained with yellow and red iron oxides. Creek Formation is recognized as an unconformity at the Paleontologic data from the studied cores suggest a Millhaven and Girard sites. This boundary is placed at the Campanian age for the Black Creek Group (Frederiksen and sharp contact at 322 ft in the Millers Pond core in this report A12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

on the basis of projecting the contact from the downdip ELLENTON FORMATION Girard core. The Ellenton Formation in the Georgia cores is finer Most of the sediments in the Steel Creek Formation are grained, calcareous, and very glauconitic in the downdip barren of fossils. Thin beds of brownish-gray clay in the Millhaven and Girard cores. It is coarser grained and non- Steel Creek section of the Millhaven core yielded Creta calcareous in the updip Millers Pond core (fig. 6). Lag ceous and Paleocene palynomorphs, but more diagnostic deposits and sharp bedding contacts identify basal uncon taxa were not recovered (Frederiksen and others, this vol formities and possible unconformities within the Georgia ume, chap. C). The presence of dinoflagellates and Pale sections. ocene palynomorphs in samples collected from the Steel The Ellenton Formation in the Millhaven core consists Creek section in the Millhaven core is discounted as con of glauconitic, calcareous, fine to coarse sand and laminated tamination of the samples with drilling mud (Edwards and clay from 642 to 622 ft; well-laminated, slightly calcareous, others, this volume, chap. B). Paleontologic data from the silty black clay from 622 to 595 ft; and calcareous to non- underlying Black Creek Group and the overlying Ellenton calcareous clay from 595 to 570 ft (fig. 3). The Ellenton Formation restrict the age of the Steel Creek Formation to Formation in the Girard core consists of noncalcareous sand the Maastrichtian. and black clay from 542 to 518 ft; sandy carbonate and Prowell, Christopher, and others (1985) identified a limestone and calcareous sand with abundant glauconite correlative section in wells at the SRS as middle from 518 to 491 ft; and well-laminated, noncalcareous silty Maastrichtian in age and designated it as unit UK6. They clay from 491 to 481 ft (fig. 4). The section generally con considered unit UK6 to be a biostratigraphic equivalent of tains well-sorted, fine to medium quartz sand. The lag the Providence Sand and part of the Ripley Formation in deposits at 638, 625, and 595 ft in the Millhaven core and 518 ft in the Girard core contain 10 to 20 percent glauconite, Georgia and the Peedee Formation in eastern South several rounded phosphatic clasts, and shark teeth. A Carolina (fig. 2). Fallaw and Price (1995) described and high-angle shear defines a sharp contact at 491 ft in the named the Steel Creek Formation at the SRS. Huddlestun Girard core. and Summerour (1996) also applied the name Steel Creek Formation to cored sections in east-central Georgia and The Ellenton Formation in the updip Millers Pond core considered the Steel Creek Formation to be early consists of fine to very coarse sand with interbedded sandy Maastrichtian. clay from 284 to 263 ft; interlaminated black lignitic clay and very fine to medium sand from 263 to 247 ft; and fine to Marine fossils, carbonate minerals, and glauconite are medium clayey sand from 247 to 232 ft (fig. 5). The lami absent from the Steel Creek sections of the studied cores. nated black clay is very dense and may contain as much as 5 The coarse sediments, fining-upward sequences, indications percent mica. Recovery of sediment in the Millers Pond of rooting, and iron-oxide staining suggest channel and core was not as good as recovery in the Millhaven and overbank deposits in a delta-plain environment. Girard cores; however, poorly sorted pebble lag deposits at 284 and 271 ft and clay clasts at 263 and 244 ft suggest pos sible unconformities and reworking of the Ellenton Forma TERTIARY STRATIGRAPHY tion in the Millers Pond core. Paleontologic results suggest that the Ellenton Forma The Tertiary section in this report includes the Ellenton tion in this report is equivalent to unit PI (Prowell, Christo and Snapp Formations in the Paleocene strata and the Four- pher, and others, 1985) and the Ellenton Formation in South mile Branch/Congaree/Warley Hill unit, the Santee Lime Carolina (Prowell, Edwards, and Frederiksen, 1985). Hud stone, and the Barnwell unit in the Eocene and younger dlestun and Summerour (1996) described a unit that they strata (fig. 2). Each of the Eocene units in the Georgia cores identified as the Black Mingo Formation undifferentiated in can be lithologically, geophysically, or biostratigraphically Georgia. They recognized a lower and an upper unit that correlated with more than one formal formation in the study resemble lithologies of the Rhems, Williamsburg, and Lang area and is informally named in the report. Syne Formations of the Black Mingo Group (Van Nieuwen- huise and Colquhoun, 1982). Fallaw and Price (1995) The stratigraphy proposed by Prowell, Christopher, divided the Ellenton section into the Sawdust Landing and and others (1985) at the southeastern corner of the SRS Lang Syne Formations in wells near the southeastern border included two Paleocene units designated as units PI and P2, of the SRS. The noncalcareous, nonglauconitic sand and six Eocene units designated as units El, E3, E4, E5, E7, and clay from 542 to 518 ft at Girard and from 284 to 263 ft at E8, and an Oligocene unit designated as unit Ol. Units E2, Millers Pond are lithologically similar to the Sawdust Land E6, and Ml were recognized and correlated in Georgia but ing Formation. However, a similar lithologic unit was not were not correlated with units in the southeastern corner of recognized at Millhaven. The rest of the Ellenton Formation the SRS (Prowell, Christopher, and others, 1985). at Millhaven and Girard is similar to the very glauconitic STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA Al3 and silty lithologies of the Lang Syne Formation. The car of Snapp sediments in the McBean core indicates that the bonate component at Millhaven and Girard is not described updip limit is irregular in that it trends to the northwest from in the Lang Syne Formation at the SRS but is described as the Thompson Oak test hole across the northern part of part of this unit beneath Allendale County in South Carolina Burke County, Ga. (fig. 1). (Fallaw and Price, 1995; Gellici and others, 1995). Paleontologic samples were not collected from the Paleontologic studies identified a diverse microflora of Snapp Formation in the Girard and Millers Pond cores dinoflagellates, pollen, and calcareous nannofossils and a because of the extensive oxidation of the sediments. A sam faunal component of ostacodes, planktonic foraminifers, ple from the base of this formation in the Millhaven core pelecypods, and gastropods in the downdip sections yielded sparse dinoflagellates that are not age diagnostic (Edwards and others, this volume, chap. B). The updip sec (Edwards and others, this volume, chap. B). The strati- tion at Millers Pond contains a low-diversity microflora of graphic position of this unit between the Ellenton Formation dinoflagellates and pollen (Clarke and others, 1994). The and the overlying early Eocene part of the Fourmile marine fossils, glauconite, and carbonate in downdip sedi Branch/Congaree/Warley Hill unit suggests that the age of ments indicate an open-marine environment, possibly distal the strata is either late Paleocene (Prowell, Christopher, and prodelta. The low diversity and the low abundance of others, 1985; Fallaw and Price, 1995) or early Eocene (Har dinoflagellates and the absence of other marine indicators at ris and Zullo, 1992). Paleontologic data from a sample at Millers Pond suggest a change to a more restricted mar 264 ft in the McBean core indicated a Paleocene age; how ginal-marine environment. ever, the authors have not independently verified that the sample at 264 ft is from the Snapp Formation. This sample of the McBean core is above the base of the Snapp Forma SNAPP FORMATION tion as selected by Huddlestun and Summerour (1996). Sedimentary characteristics suggest a fluvially domi The Snapp Formation at Millhaven, Girard, and Mill nated depositional environment in either an upper delta ers Pond consists of moderately to poorly sorted, fine to plain or an incised alluvial valley. The presence of very coarse sand overlain by iron-stained, oxidized kaolin dinoflagellates in the Millhaven core suggests a mar (figs. 3, 4, 5). The sand is unlithified and generally has gran ginal-marine environment in the downdip part of the study ules, pebbles, and less than 10 percent clay matrix. Individ area. The Snapp Formation at Girard is 58 ft thick, which is ual sand beds typically are coarse to very coarse in the lower roughly 20 ft thicker than the Snapp Formation in cores part of each section. In the middle of each section, the sand from the southeastern part of the SRS. The thicker section beds are fine to medium. At the top of each section, the sand of the Snapp Formation in the Girard core overlies a section beds grade into white to very light gray kaolin. The clay is of the Ellenton Formation that is thinner by 20 ft relative to stained with red and yellow iron oxides. Pedogenic struc the Ellenton section in the southeastern part of the SRS. tures in the otherwise massive clay include root traces and Structural-contour and isopach maps of the Black Mingo desiccation cracks. Pyrite is disseminated in the clay and (Ellenton) and Snapp Formations also indicate thicker sec along desiccation cracks near the top of the Snapp Forma tions of the Snapp Formation over thinner sections of the tion in the Millers Pond and Girard cores. Black Mingo (Ellenton) Formation in eastern Burke County The Snapp Formation in Georgia is equivalent to unit and southern Barnwell County (Huddlestun and Summer P2 (Prowell, Christopher, and others, 1985) and the Snapp our, 1996). This thickness change is interpreted here as evi Formation at the SRS (Fallaw and Price, 1995). McClelland dence of channel incision of the Snapp Formation into the (1987) applied the name Rhems Formation (lower Pale- laminated black clay of the Ellenton Formation. ocene part of the Black Mingo Group) to a combined sec tion of the Snapp and Ellenton Formations in upper Burke County. The Snapp Formation holds the same upper Pale- FOURMILE BRANCH/CONGAREE/WARLEY HILL UNIT ocene stratigraphic position as the Chicora Member of the Williamsburg Formation of the Black Mingo Group (Van The lithologies of the Fourmile Branch/Congaree/War- Nieuwenhuise and Colquhoun, 1982). The Snapp Formation ley Hill unit range from mixed-siliciclastic-carbonate sec in the Georgia cores and in cores on the SRS (Fallaw and tions in the central and downdip Georgia cores to Price, 1995) is lithologically different from the marine sedi siliciclastic sections in the updip cores (figs. 3, 4, 5, 6). ment of the Chicora Member. Paleontologic data suggest that the strata in this unit are cor The Snapp Formation is absent from the Thompson relative with three formally named formations at the SRS Oak core (fig. 1, table 1). Fallaw and Price (1995) described (fig. 2). However, all three formations are not consistently an updip limit for the Snapp Formation near the Upper present in each of the Georgia cores (table 1). Three Runs Creek in Aiken County, S.C. Extension of this In the downdip Millhaven core, the Fourmile Branch/ boundary into Georgia would place the Thompson Oak core Congaree/Warley Hill unit consists of interbedded quartz near the updip limit of the Snapp Formation. The presence sand, marl, and limestone. The sand is very fine to fine A14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA below a depth of 415 ft and fine to medium above a depth of from 274 to 251 ft (Edwards, this volume, chap. G). These 415 ft and is moderately to well sorted throughout. Glauco- sections in the Girard and Thompson Oak cores appear to be nite is a common accessory mineral and is abundant at 462 equivalent to unit E2 of Prowell, Christopher, and others ft. The carbonate beds range from lithified to unlithified and (1985) and the Fourmile Branch Formation at the SRS (Fal include glauconite, clay matrix and fossils. Extensive bur law and Price, 1995). A biostratigraphically correlative sec rowing is recognized in the sandy carbonate matrix. tion was not identified at Millhaven, Millers Pond, or In the Girard core, this unit consists of medium to McBean. coarse sand from 423 to 390 ft; fine to medium sand from The section from 390 to 325 ft in the Girard core is 366 to 350 ft; and medium to coarse sand, sandy carbonate, biostratigraphically correlative with the sections from 504 and limestone from 342 to 325 ft. A large part of the unit to 462 ft in the Millhaven core and from 165 to 156 ft in the from 390 to 366 ft and several other parts of the section Millers Pond core, and with samples collected from depths were not recovered during coring. The section below 390 ft of 210, 194, 192, and 183 ft in the Thompson Oak core. is predominantly noncalcareous with only trace amounts of This part of the Fourmile Branch/Congaree/Warley Hill unit glauconite, generally less than 5 percent clay matrix, clay is equivalent to unit E3 (Prowell, Christopher, and others, laminae, and clay-lined burrows. Unlithified sandy carbon 1985) and the Congaree Formation in South Carolina (Fal ate and partially lithified calcareous sand are abundant law and Price, 1995) and Georgia (Huddlestun and Sum- above 366 ft. merour, 1996). This unit in the Millers Pond core consists of a 9-ft The Fourmile Branch/Congaree/Warley Hill section section of well-sorted, very fine to fine sand. The sand con from 462 to 401 ft in the Millhaven core is lithologically tains less than 5 percent clay matrix, but clay-lined burrows equivalent and geophysically correlative with at least part of are present. the Congaree Formation as identified in the subsurface of Surface mapping and drill hole evidence from this Allendale County in South Carolina (Gellici and others, updip region in Georgia and adjacent areas of South Caro 1995). This section is biostratigraphically equivalent to the lina indicate a thicker section of sand and clay (Nystrom and lower part of unit E4 (Prowell, Christopher, and others, Willoughby, 1982; Nystrom and others, 1986; McClelland, 1985) and the Warley Hill Formation at the SRS (Fallaw and 1987; Prowell, 1994). On the basis of data from augered Price, 1995). A biostratigraphic equivalent to this part of the holes that are 1 mile west of the Millers Pond core site, Fourmile Branch/Congaree/Warley Hill section is not iden McClelland (1987) described a 40-ft section of the Huber tified in the other studied cores in Georgia. Formation, a time-equivalent lithofacies of the Congaree Sedimentary characteristics of the Fourmile Branch Formation. In the Huber Formation described by McClel sections in the Girard and Thompson Oak cores suggest a land (1987), the burrowed, fine sand observed at Millers nearshore-marine environment. Sedimentary characteristics Pond is overlain by a crossbedded, fine to coarse quartz of the overlying Congaree beds suggest an open-marine sand and lenticular beds of massive, lignitic kaolinitic clay. shelf environment for deposits in the downdip core and a Dinoflagellates, pollen, and calcareous nannofossils fluvially dominated to marginal-marine environment for were recovered from the core samples of the Fourmile deposits in the updip cores in the vicinity of Millers Pond. Branch/Congaree/Warley Hill unit at Millhaven and Girard. The Warley Hill Formation at Millhaven also was deposited Dinoflagellates and pollen were recovered from the Thomp in an open-marine shelf environment. son Oak and Millers Pond cores. Paleontologic examination of these core samples indicates that this unit is early Eocene to early middle Eocene in age and that it includes more than SANTEE LIMESTONE one biostratigraphic unit (Bybell, this volume, chap. F; Fre- deriksen, this volume, chap. H; Edwards, this volume, chap. The Santee Limestone consists predominantly of lime G). Other fossils observed in the Millhaven core included stone and unlithified carbonate with a few beds of calcare bryozoans, pelecypods, and foraminifers below 462 ft and ous sand and clay. The Santee Limestone, as correlated in pelecypods and foraminifers above 462 ft. In the Girard this report, includes lithologies assigned by others to the core, pelecypods, bryozoans, and shark teeth were observed Warley Hill Formation (Steele, 1985; McClelland, 1987; above 342 ft. Biomoldic pores indicate that gastropods also Fallaw and Price, 1992, 1995), the Blue Bluff Marl of the were present. Lisbon Formation (Huddlestun and Hetrick, 1986), the San The Fourmile Branch/Congaree/Warley Hill unit from tee Limestone (Sloan, 1908), and the McBean Formation 423 to 390 ft in the Girard core is lithologically and geo- (Veatch and Stephenson, 1911). These lithofacies are time physically correlative with the Fourmile Branch Formation equivalents of the Lisbon Formation of western Georgia at the SRS (Fallaw and Price, 1995). The age of this part of (Prowell, Christopher, and others, 1985) and collectively are the Girard core could not be determined from fossil evi correlated as one package of sediment in this report (fig. 6), dence. An early Eocene age was determined with although we do recognize significant stratigraphic contacts dinoflagellates from samples of the Thompson Oak core within the unit. STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A15

The lower part of the Santee Limestone in the Mill- include oysters and other pelecypods, foraminifers, and haven core from a depth of 401 to 365 ft consists of calcare echinoid fragments. Biomoldic porosity also is present ous sand with glauconite and pelecypods that grades into above a depth of 100 ft and reflects dissolution of aragonitic overlying sandy carbonate with large oyster shells and other pelecypods and gastropods. pelecypods (fig. 3). The quartz sand is medium to coarse The Santee Limestone at Millers Pond is thicker than near the base of the section and fines upward to fine to comparable sections in this updip area (Nystrom and Wil- medium. The carbonate in this part of the section ranges loughby, 1982; Nystrom and others, 1986; McClelland, from unlithified to partially lithified. The contact between 1987; Prowell, 1994). McClelland (1987) described this unit the lower and middle part of the section at 365 ft is phos- as 40 ft thick in a drill hole located west of the Millers Pond phatized and pyritized. Pelecypod-moldic pores immedi site. This information, in conjunction with the evidence for ately beneath the contact are filled with the very fine the section missing from the underlying Fourmile sediments of the overlying marl. Branch/Congaree/Warley Hill Formation, suggests that the The middle part of the Santee Limestone in the Mill- basal contact of the Santee Limestone represents scour into haven core from 365 to 245 ft varies from marl to carbonate the underlying unit and is possibly the result of localized with very little quartz sand in both lithologies. Carbonate channeling. Observations of similar channeling have been from 365 to 268 ft is well lithified and has biomoldic poros reported in nearby strip mines (Nystrom and others, 1986). ity. The marl is burrow mottled to wavy laminated with The Santee Limestone section from 156 to 139 ft in the minor amounts of lignite and pyrite. Fossils in the marl Millers Pond core is biostratigraphically correlative with include foraminifers, spicules, shark teeth, pelecypods, and sections in the Millhaven core from 401 to 365 ft and in the gastropods. The marl grades into overlying well-lithified to Girard core from 325 to 322 ft and with samples collected at partially lithified limestone. Fossils in the limestone are depths of 181.5, 174, 172, 164 and 154 ft in the Thompson more abundant and more diverse than in the marl and Oak core and 181 ft in the McBean core (Edwards, this vol include pelecypods, gastropods, bryozoans, echinoids, fora ume, chap. G; Bybell, this volume, chap. F; Frederiksen, minifers, brachiopods, and shark teeth. A sharp bedding this volume, chap. H). This part of the Santee Limestone in contact at 332 ft is underlain by biomoldic limestone with the studied cores is biostratigraphically equivalent to the phosphatized fossil molds and shark teeth from 336 to 332 upper part of the unit E4 (Prowell, Christopher, and others, ft. Porosity in the middle part of the section is interparticle 1985). Prowell, Christopher, and others (1985) identified and biomoldic with irregular dissolution cavities from 258 their unit as correlative with part of the Warley Hill Forma to 252 ft. tion underlying the southeastern part of the SRS. Gellici and The sandy carbonate in the upper part of the Santee others (1995) described a similar lithologic unit in the same Limestone in the Millhaven core from 245 to 228 ft includes stratigraphic position in the subsurface of Allendale County fine to medium quartz sand and glauconite. Marine fossils and designated the unit as the Warley Hill Formation. Steele include pelecypods, bryozoans, and gastropods. (1985) and McClelland (1987) described a calcareous litho- The Santee Limestone in the Girard core includes a facies of the Warley Hill Formation. Fallaw and Price very sandy limestone from 325 to 322 ft and a marl and (1995) described a sporadic sand lithofacies of the Warley clayey sand from 322 to 250 ft (fig. 4). The limestone from Hill Formation at the base of the Tinker Formation in the 325 to 322 ft is glauconitic with abundant pelecypod-moldic updip part of the SRS. porosity and is pyritic along the contact with the overlying The remainder of the Santee Limestone in the Mill- marl. The marl is a very fine grained limestone unit with as haven, Girard, and Millers Pond cores is biostratigraphically much as 30 percent clay matrix. Very fine to fine quartz equivalent to unit E5 (Prowell, Christopher, and others, sand ranges from 2 percent near the base of the section to 25 1985) and the Tinker Formation (Fallaw and Price, 1995). percent near the top of the section. The marl and calcareous This part of the Santee Limestone is lithologically similar to sand are burrow mottled and contain minor amounts of lig the Blue Bluff Marl of the Lisbon Formation (Huddlestun nite and glauconite. Macrofossils are sparse and include and Hetrick, 1986), the Santee Limestone (Sloan, 1908), pelecypods. and the McBean Formation (Veatch and Stephenson, 1911). The Santee Limestone in the Millers Pond core con The siliciclastic lithologies of the Tinker Formation in South sists of sandy limestone and calcareous sand (fig. 5). A thin Carolina (Fallaw and Price, 1995) are correlative with the basal lag of very poorly sorted sand from 156 to 154 ft predominantly carbonate lithologies of the Santee Lime includes quartz pebbles and granules, glauconite, and pele stone but are not recognized in the Georgia cores. cypods. The quartz sand above 154 ft is fine to very coarse Calcareous nannofossils, planktonic foraminifers, in calcareous sand beds and fine to medium in sandy lime dinoflagellates, and pollen from the core localities indicate a stone beds. The limestone below a depth of 121 ft is finely late middle Eocene (late Claibornian) age for the Santee crystalline and contains glauconite and marine fossils, sections (Edwards and others, this volume, chap. B). Marine including pelecypods, spicules, foraminifers, and shark fossils and carbonate suggest that this unit was deposited in teeth. Marine fossils in the limestone above a depth of 100 ft an open-marine, shallow-shelf environment. The distribu- A16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA tion of siliciclastic sediments and the diversity of marine The Barnwell unit at Millers Pond consists of silici fossils in the carbonate facies suggest that the updip Millers clastic sediments from a depth of 82 ft to land surface. The Pond core is more proximal to a source of siliciclastic sedi contact with the Santee Limestone was not recovered in cor ments than the downdip Millhaven core. ing. A thin, irregularly shaped bed of limestone at 75 ft is lithologically similar to the underlying Santee Limestone and is presumed to be a large reworked clast. The Barnwell BARNWELL UNIT unit from 78 to 67 ft includes thin beds of fine to medium and fine to very coarse sand, and thin beds of well-lami The Barnwell unit derives its name from the Barn well Group (Huddlestun and Hetrick, 1979, 1986). The Barnwell nated clay. The sand has fine lignite, clay clasts, and 10 to Group consists of the Clinchfield Formation, Dry Branch 20 percent clay matrix. The section from 67 ft to land sur Formation, and Tobacco Road Sand that have been face is a coarsening-upward sequence of sand and ranges described and mapped on both sides of the Savannah River from fine to medium sand up to fine to very coarse sand. in the vicinity of the SRS (Huddlestun and Hetrick, 1978, The amount of clay matrix ranges from 5 to 25 percent. Sed 1979, 1986; Huddlestun, 1982; Prowell, 1994; Fallaw and imentary structures include clay laminae and clay wisps Price, 1995). The informally named Barnwell unit in this from 66 to 62 ft, 48 to 47 ft, and 38 to 27 ft. The sand from report includes strata of the Barnwell Group and the 49 to 42 ft contains granules and pebbles. The Barnwell unit post-Eocene strata in the study area. is mapped as the uppermost stratigraphic unit at the Millers The Barnwell unit in the Millhaven core includes cal Pond site (Prowell, 1994), where it includes the Tobacco careous clay from a depth of 228 to 223 ft, and moderately Road Sand and Irwinton Sand Member of the Dry Branch well to well-sorted calcareous quartz sand and partially lith- Formation. Partial recovery of sediments during coring ified sandy limestone from 223 to 123 ft (fig. 3). The fine to makes selection of a formation contact within the Barnwell medium sand includes 1 percent glauconite. Thin beds of unit difficult. silica-replaced limestone are common from a depth of 200 The contact between the Barnwell Group and a to 170 ft. The section from 123 to 54 ft consists of unlithi- post-Eocene unit, as mapped in the area of the Girard site fied carbonate and partially lithified limestone with gener (Prowell, 1994), was not identified in the Girard core. The ally less than 10 percent quartz sand and 1 percent glauconite. Irregularly shaped phosphatized limestone clasts post-Eocene unit was described and designated as map unit at the base of this part of the section produce a sharp spike Tu (Prowell, 1994). The mapped contact was projected to a on the gamma-ray log at 123 ft. The unit from 54 ft to land depth of 50 ft in the Girard section. A lag deposit and other surface consists of a coarsening-upward sequence of clayey evidence of an unconformity, if present in the Girard sec sand and sandy clay. Fossils observed in the core include tion, were not recovered during coring at this depth. The pelecypods, bryozoans, echinoids, and foraminifers from presence of post-Eocene sediments is acknowledged at the 223 to 54 ft. Biomoldic pores are present from 67 to Girard site on the basis of previous studies, but a separate 34 ft and reflect dissolution of aragonitic pelecypods and unit is not defined at this time. gastropods. Paleontologic data for the Millhaven and Girard cores The Barnwell unit in the Girard core consists of clay, suggest a late Eocene to questionably early Oligocene age sand, and carbonate lithologies in the lower part of the sec for the Barnwell sections (Edwards and others, this volume, tion from 250 to 104 ft and sand and clay in the upper part chap. B). The Barnwell unit is equivalent to units E6, E7, of the section from 104 ft to land surface (fig. 4). A basal E8, and Ml (Prowell, Christopher, and others, 1985) and the calcareous clay from 250 to 244 ft is overlain by partially Clinchfield Formation, Dry Branch Formation, and Tobacco silicified, phosphatized, and glauconitic limestone from a Road Sand of the Barnwell Group at the SRS (Fallaw and depth of 244 to 234 ft; calcareous quartz sand from 234 to Price, 1995). Throughout the study area, the abundance of 193 ft; sandy limestone from 193 to 183 ft; marl from 183 to carbonate, the presence of glauconite and phosphate, and 136 ft; and a sandy limestone that grades into an overlying quartz sand from 136 to 104 ft. Fossils include pelecypods the abundance of marine macrofossils and microfossils in and bryozoans. Biomoldic porosity ranges from 5 to 20 per the calcareous part of the section indicate that the Barnwell cent in the limestone and reflects dissolution of aragonitic strata were deposited in open-marine environments. The pelecypods. Sand is fine to coarse near the base and very calcareous sand probably was deposited in a shallow-shelf fine to fine in the rest of the section from 250 to 104 ft. Clay environment, and the fossil bed at the base is a lag deposit matrix ranges from 20 to 40 percent in the sand. Clay lami produced by a late Eocene marine transgression. The non- nae are abundant below 172 ft. The Barnwell unit from 104 calcareous sand and clay, the ovoid flattened pebbles, and ft to land surface is noncalcareous and contains clayey sand the clay wisps in the upper part of the Barnwell unit sug and clay. The sand ranges from fine to coarse and contains gest that these strata were deposited in nearshore-marine several flattened, ovoid pebbles at 88 ft. environments. STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF SEDIMENTS FROM FIVE CORES, GEORGIA A17

SUMMARY ence on deposition in the downdip area near Millhaven. Dif ferences in the thickness of this formation in the study area Five deep stratigraphic test holes were drilled from suggest that channels containing the basal sand of the Snapp 1991 to 1993 in support of multidisciplinary investigations Formation are incised into laminated black clay of the to determine the stratigraphy of Upper Cretaceous and Ter Ellenton Formation. tiary sediments of the coastal plain in east-central Georgia. The lithologies of the Fourmile Branch/Congaree/War Cored sediment and geophysical logs from the Millhaven ley Hill unit range from mixed-siliciclastic-carbonate sec test hole in Screven County and the Girard and Millers Pond tions in the central and downdip Georgia cores to test holes in Burke County are the primary sources of litho- siliciclastic sections in the updip cores. Paleontologic data logic and paleontologic information for this report. Litho- suggest that the strata in this unit are correlative with three logic and paleontologic information from the Thompson formally named formations at the SRS. However, all three Oak and McBean test holes in Burke County supplement the formations are not consistently present in each of the Geor discussion of stratigraphy and sedimentation in the updip gia cores. part of the study area near the Millers Pond test hole. The Santee Limestone consists predominantly of lime The Cretaceous sections in the studied cores are stone and unlithified carbonate with a few beds of calcare divided into the Cape Fear Formation, the Middendorf For ous sand and clay. The Santee Limestone, as correlated in mation, the Black Creek Group, and the Steel Creek Forma this report, includes lithologies assigned by others to the tion. These four geologic units consist of siliciclastic Warley Hill Formation, the Blue Bluff Marl of the Lisbon sediments. Evidence of possible unconformities is used to Formation, the Santee Limestone, and the McBean Forma recognize two subunits in the Middendorf Formation and tion. These lithofacies are time equivalents of the Lisbon three subunits in the Black Creek Group. Sediments in the Formation of western Georgia and collectively are corre Cretaceous section generally are coarser grained and more lated as one package of sediment in this report. oxidized in updip areas. Each contact between units is con sidered to be a regional unconformity and denotes a consid The informally named Barnwell unit in this report erable hiatus in sedimentation. The sediments in all four includes strata of the Barnwell Group and the post-Eocene units have been interpreted as being part of large deltaic sys strata in the study area. The presence of post-Eocene sedi tems that prograded across the paleo-continental shelf in ments is acknowledged at the Girard site on the basis of pre east-central Georgia and western South Carolina. The litho- vious studies, but a separate unit is not defined at this time. facies observed in the Upper Cretaceous units tend to be coarser grained in proximal-deltaic environments and finer grained in distal-deltaic environments. REFERENCES CITED The Tertiary sections are divided into the Ellenton and Snapp Formations of Paleocene age; the Fourmile Bechtel Corporation, 1972, Applicants environmental report, vol Branch/Congaree/Warley Hill unit and Santee Limestone of umes I and II—Alvin W. Vogtle Nuclear Plant: unpublished report for Georgia Power Company, Atlanta, Georgia; report Eocene age; and the Barnwell unit, which contains strata of on file at U.S. Geological Survey, Doraville, GA 30360. Eocene to Miocene age. The Tertiary section, with the ————1973, Preliminary safety analysis report, volumes II and exception of the Snapp Formation, generally is more calcar III—Alvin W. Vogtle Nuclear Plant: unpublished report for eous and has a more diverse and abundant marine micro- Georgia Power Company, Atlanta, Georgia; report on file at flora and fauna in the downdip Millhaven core, relative to U.S. Geological Survey, Doraville, GA 30360. the updip McBean and Millers Pond cores. For these units, -1982, Studies of postulated Millett fault, Georgia Power sedimentary and paleontologic evidence suggests open- Company Vogtle Nuclear Plant: San Francisco, Bechtel Cor marine shelf environments at the Millhaven site and mar poration, unpublished report, volumes 1 and 2, variously ginal-marine environments at the Millers Pond site. paged. 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Sedi III: E.I. du Pont de Nemours and Company, Savannah River mentary characteristics of the Snapp Formation suggest a Laboratory, Aiken, S.C., DPST-88-627, 294 p. fluvially dominated depositional environment such as an Brantley, I.E., 1916, A report on the limestones and marls of the upper delta plain or an incised alluvial valley. The presence coastal plain of Georgia: Georgia Geological Survey Bulletin of a sparse marine microflora suggests some marine influ 21, 300 p. A18 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

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(v. 1, Plains: Proceedings of the Second Bald Head Island Confer 467 p., v. 2, 231 p.). ence on Coastal Plains Geology, Hilton Head Island, Novem Kidd, N.B., 1996, Determination of the hydraulic properties of ber 6-11, 1990, p. 134-142. coastal plain aquifers at Millers Pond and Millhaven, Herrick, S.M., 1960, Some small Foraminifera from Shell Bluff, east-central Georgia: Clemson, S.C., Clemson University, Georgia: Bulletins of American Paleontology, v. 41, p. 1 IT- M.S. thesis, 153 p. 127. LaMoreaux, P.E., 1946a, Geology and ground-water resources of ————1961, Well logs of the coastal plain of Georgia: Georgia the coastal plain of east-central Georgia: Georgia Geologic Geologic Survey Bulletin 70, 462 p. Survey Bulletin 52, 173 p. ————1946b, Geology of the coastal plain of east-central Geor ————1964, Upper Eocene small Foraminifera from Shell Bluff gia: Georgia Geologic Survey Bulletin 50, 26 p. and Griffins Landing, Burke County, Georgia: U.S. Geologi Leeth, D.C., Falls, W.F., Edwards, L.E., Frederiksen, N.O., and cal Survey Professional Paper 501-C, p. C64-C65. Fleming, R.F., 1996, Geologic, hydrologic, and water-chem -1972, Age and correlation of the Clinchfield Sand of Geor istry data for a multi-aquifer system in coastal plain sediments gia: U.S. Geological Survey Bulletin 1354-E, 17 p. near Girard, Burke County, Georgia, 1992-95: Georgia Geo Herrick, S.M., and Counts, H.B., 1968, Late Tertiary stratigraphy logic Survey Information Circular 100, 26 p., 1 pi. in pocket. of eastern Georgia: Georgia Geological Society, 3d Field Trip Leeth, D.C., and Nagle, D.D., 1996, Shallow subsurface geology Guidebook, 88 p. of part of the Savannah River alluvial valley in the upper Herrick, S.M., and Vorhis, R.C., 1963, Subsurface geology of the coastal plain of Georgia and South Carolina: Southeastern Georgia Coastal Plain: Georgia Geologic Survey Information Geology, v. 36, no. 1, p. 1-14. Circular 25, 78 p. LeGrand, H.E., and Furcon, A.S., 1956, Geology and Hetrick, J.H., 1992, A geologic atlas of the Wrens-Augusta area: ground-water resources of central-east Georgia: Georgia Geo Georgia Geologic Survey Geologic Atlas 8, 3 pis. logic Survey Bulletin 64, 164 p. Huddlestun, P.P., 1982, The development of the stratigraphic ter Logan, W.R., and Euler, G.M., 1989, Geology and ground-water minology of the Claibornian and Jacksonian marine deposits resources of Allendale, Bamberg, and Barnwell Counties and of western South Carolina and eastern Georgia, in Nystrom, part of Aiken County, South Carolina: South Carolina Water P.G., Jr., and Willoughby, R.H., eds.. Geological investiga Resources Commission Report 155, 113 p. tions related to the stratigraphy in the kaolin mining district, Marine, I.W, 1979, Hydrology of buried crystalline rocks at the Aiken County, South Carolina (Carolina Geological Society Savannah River Plant near Aiken, South Carolina: U.S. Geo Field Trip Guidebook for 1982): Columbia, S.C., South Caro logical Survey Open-File Report 79-1544, 160 p. lina Geological Survey, p. 21-33. Marine, I.W., and Siple, G.E., 1974, Buried Triassic basin in the ————1988, A revision of the lithostratigraphic units of the central Savannah River area, South Carolina and Georgia: coastal plain of Georgia, Miocene through Holocene: Georgia Geological Society of America Bulletin, v. 85, p. 311-320. Geologic Survey Bulletin 104, 162 p. McClelland, S.A., 1987, Surface and subsurface stratigraphy of ————1992, Upper Claibornian coastal marine sands of eastern Cretaceous and younger strata along the Savannah River from Georgia and the Savannah River area, in Fallaw, W.C., and southern Richmond County through Burke County, Georgia: Price, Van, eds., Geological investigations of the central Columbia, S.C., University of South Carolina, M.S. thesis, Savannah River area, South Carolina and Georgia (Carolina 123 p. Geological Society field trip guidebook, November 13-15, Nystrom, P.G., Jr., and Willoughby, R.H., eds., 1982, Geological 1992): U.S. Department of Energy and South Carolina Geo investigations related to the stratigraphy in the kaolin mining logical Survey, p. CGS-92-B.XII.1-B.XII.6. district, Aiken County, South Carolina (Carolina Geological A20 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Society Field Trip Guidebook for 1982): Columbia, S.C., Siple, G.E., 1967, Geology and ground water of the Savannah South Carolina Geological Survey, 183 p. River Plant and vicinity. South Carolina: U.S. Geological Sur Nystrom, P.G., Jr., Willoughby, R.H., and Kite, L.E., 1986, Creta vey Water-Supply Paper 1841, 113 p. ceous-Tertiary stratigraphy of the upper edge of the coastal Sloan, Earle, 1908, Catalogue of mineral localities of South Caro plain between North Augusta and Lexington, South Carolina lina: South Carolina Geological Survey, ser. 4, Bulletin 2, p. (Carolina Geological Society Field Trip Guidebook for 1986): 449-^53. Columbia, S.C., South Carolina Geological Survey, 82 p. Smith, G.E., III, 1979, Stratigraphy of the Aiken County Coastal Nystrom, P.G., Jr., Willoughby, R.H., and Price, L.K., 1991, Creta Plain: South Carolina Geological Survey Open-File Report ceous and Tertiary stratigraphy of the upper coastal plain, 19, 34 p. South Carolina, in Horton, J.W., Jr., and Zullo, V.A., eds., Geology of the Carolinas: Knoxville, Tenn., University of Snipes, D.S., 1965, Stratigraphy and sedimentation of the Midden- Tennessee Press, p. 221-240. dorf Formation between Lynches River, South Carolina, and Owens, J.P., 1989, Geologic map of the Cape Fear region, Florence the Ocmulgee River, Georgia: Chapel Hill, N.C., University I°x2° quadrangle and northern half of the Georgetown I°x2° of North Carolina, Ph.D. dissertation, 140 p. quadrangle, North Carolina and South Carolina: U.S. Geolog Snipes, D.S., Fallaw, W.C., Price, Van, and Cumbest, R.J., 1993, ical Survey Miscellaneous Investigations Series Map 1-1948- The Pen Branch fault; documentation of Late Cretaceous-Ter A, 2 sheets, scale 1:250,000. tiary faulting in the coastal plain of South Carolina: South Price, Van, Fallaw, W.C., and McKinney, J.B., 1991, Geologic set eastern Geology, v. 33, no. 4, p. 195-218. ting of the new production reactor reference site with the Sohl, N.F., and Owens, J.P., 1991, Cretaceous stratigraphy of the Savannah River Site (U): Westinghouse Savannah River Com Carolina Coastal Plain, in Horton, J.W, Jr., and Zullo, V.A., pany-Savannah River Site, Report WSRC-RP-91-96, 80 p. eds., Geology of the Carolinas: Knoxville, Tenn., University Prowell, D.C., 1994, Preliminary geologic map of the Barnwell of Tennessee Press, p. 191-220. 30'x60' quadrangle, South Carolina and Georgia: U.S. Geo Steele, K.B., 1985, Lithostratigraphic correlation of Cretaceous logical Survey Open-File Report 94-673, 88 p. and younger strata of the Atlantic Coastal Plain Province Prowell, D.C., Christopher, R.A., Edwards, L.E., Bybell, L.M., and within Aiken, Allendale and Barnwell Counties, South Caro Gill, H.E., 1985 [1986], Geologic section of the updip coastal lina: Columbia, S.C., University of South Carolina, M.S. the plain from central Georgia to western South Carolina: U.S. sis, 174 p. Geological Survey Miscellaneous Field Studies Map MF- 1737, 10-p. text, 1 sheet. Summerour, J.H., Shapiro, E.A., Lineback, J.A., Huddlestun, P.P., and Hughes, A.C., 1994, An investigation of tritium in the Prowell, D.C., Edwards, L.E., and Frederiksen, N.O., 1985 [1986], Gordon and other aquifers in Burke County, Georgia: Georgia The Ellenton Formation in South Carolina—A revised age Geologic Survey Information Circular 95, 93 p. designation from Cretaceous to Paleocene, in Stratigraphic notes, 1984: U.S. Geological Survey Bulletin 1605-A, p. Van Nieuwenhuise, D.S., and Colquhoun D.J., 1982, The Pale- A63-A69. ocene-lower Eocene Black Mingo Group of the east-central Prowell, D.C., and O'Connors, B.J., 1978, Belair fault zone—Evi• coastal plain of South Carolina: South Carolina Geology, v. dence of Tertiary fault displacement in eastern Georgia: Geol 26, no. 2, p. 47-67. ogy, v. 6, no. 10, p. 681-684. Veatch, Otto, and Stephenson, L.W, 1911, Preliminary report on Robertson, C.G., 1990, A textural, petrographic, and hydrogeolog- the coastal plain of Georgia: Georgia Geologic Survey Bulle ical study of the Congaree Formation at the Savannah River tin 26, 446 p. Site, South Carolina: Wilmington, N.C., University of North Zullo, V.A., Willoughby, R.H., and Nystrom, P.G., Jr., 1982, A late Carolina, M.S. thesis, 65 p. Oligocene or early Miocene age for the Dry Branch Forma Schroder, C.H., 1982, Trace fossils of the Oconee Group and basal tion and Tobacco Road Sand in Aiken County, South Caro Barnwell Group of east-central Georgia: Georgia Geologic lina, in Nystrom, P.G., Jr., and Willoughby, R.H., eds., Survey Bulletin 88, 125 p. Geological investigations related to the stratigraphy in the Scrudato, R.J., and Bond, T.A., 1972, Cretaceous-Tertiary bound kaolin mining district, Aiken County, South Carolina (Caro ary of east-central Georgia and west-central South Carolina: lina Geological Society Field Trip Guidebook for 1982): Southeastern Geology, v. 14, p. 233-239. Columbia, S.C., South Carolina Geological Survey, p. 34-46. U.S. Department of the Interior U.S. Geological Survey

Overview of the Biostratigraphy and Paleoecology of Sediments from Five Cores from Screven and Burke Counties, Georgia By Lucy E. Edwards, Norman 0. Frederiksen, Laurel M. Bybell, Thomas G. Gibson, Gregory S. Gohn, David Bukry, Jean M. Self-Trail, and Ronald J. Litwin

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-B

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract...... Bl Introduction...... 1 Pollen...... 2 Dinoflagellates and Acritarchs...... 2 Calcareous Nannofossils...... 3 Ostracodes...... 3 Foraminifers...... 3 Acknowledgments...... 4 Material and Methods ...... 4 Stratigraphic Framework...... 4 Biostratigraphy and Paleoecology ...... 4 Cape Fear Formation...... 4 Middendorf Formation...... 5 Black Creek Group ...... 5 Steel Creek Formation ...... 14 Ellenton Formation...... 14 Snapp Formation...... 14 Fourmile Branch Formation...... 15 Congaree Formation...... 15 Warley Hill Formation ...... 15 Santee Limestone...... 16 BarnwellUnit...... 16 Summary and Implications ...... 16 References Cited...... 17

FIGURES

1. Index map showing the Savannah River Site and the location of test holes in the study area...... B2 2. Chart showing terminology that has been used for lithostratigraphic units in the eastern United States and our interpretations of their chronostratigraphic correlations ...... 6 3-8. Diagrams summarizing Stratigraphic and paleontologic data for three cores— 3. Tertiary part of the Millhaven core ...... 8 4. Cretaceous part of the Millhaven core...... 9 5. Tertiary part of the Girard core...... 10 6. Cretaceous part of the Girard core...... 11 7. Tertiary part of the Millers Pond core...... 12 8. Cretaceous part of the Millers Pond core...... 13

III

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Overview of the Biostratigraphy and Paleoecology of Sediments from Five Cores from Screven and Burke Counties, Georgia

By Lucy E. Edwards, Norman O. Frederiksen, Laurel M. Bybell, Thomas G. Gibson, Gregory S. Gohn, David Bukry, Jean M. Self-Trail, and Ronald J. Litwin

ABSTRACT minifers indicate inferred water depths of less than 200 ft. The Barnwell unit is difficult to date paleontologically but is late Eocene and questionably early Oligocene and is marine. Five cores from Screven and Burke Counties, Georgia, This chapter contains highlights from the individual chap form the basis for a multifaceted paleontological study of ters in this volume. Cretaceous and Tertiary coastal plain sediments. The biostratigraphy and paleoecology of these cores are summa rized within the lithostratigraphic framework given in this INTRODUCTION volume. The basal Cretaceous unit, the Cape Fear Forma tion, is of probable Coniacian age and is nonmarine. The At the Savannah River Site (SRS) in Aiken, Barnwell, Middendorf Formation may represent similar lithofacies of and Allendale Counties, S.C., various hazardous materials different ages, one representing undifferentiated pollen have been manufactured, disposed of, and stored since the Zone V (late Coniacian and Santonian) and one slightly early 1950's. Ground-water contamination has been younger (latest Santonian(?) or early Campanian). The detected on the site, and the potential exists for contamina Black Creek Group is Campanian. It is marginal marine to tion in areas adjacent to the site. In 1991, the U.S. Depart nonmarine in its lower part (subunit 1). In all but the most ment of Energy (DOE) funded a multidisciplinary study by updip core, subunit 2 of the Black Creek contains Campa the U.S. Geological Survey (USGS) to determine whether nian marine sediments. Subunit 3 of the Black Creek shows ground water flows from the SRS through aquifers in South a marine influence in the most basinward (downdip) Mill- Carolina into aquifers in Georgia and to determine under haven core. The Steel Creek Formation is Maastrichtian in what pumping scenarios such flow could occur in the future. the Millhaven core and is nonmarine except for its lowest Following the detection of tritium in a public water supply part. well in Burke County, Ga., additional DOE funding was The basal Tertiary unit, the Ellenton Formation, is of provided to the Georgia Geologic Survey (GGS) of the early, early late, and middle late Paleocene age. It is marine Georgia Department of Natural Resources for subsurface throughout the study area. The overlying Snapp Formation investigations (Clarke and others, 1994; Summerour and yields pollen of late, but not latest, Paleocene age. It is others, 1994). mostly nonmarine but contains rare marginal marine Accurate ground-water modeling in the Atlantic palynomorphs. The Fourmile Branch Formation, present Coastal Plain depends on an understanding of the stratigra only in the Girard and Thompson Oak cores, is a marine phy. Numerous investigations of subsurface stratigraphy unit of early Eocene age. The Congaree Formation is of have been conducted in western South Carolina, from Siple early middle Eocene age and is present and contains marine (1967) to Fallaw and Price (1995), but relatively little has fossils in all five cores. The middle Eocene Warley Hill For been published about the subsurface of eastern Georgia mation is present only in the Millhaven core. These sedi (Prowell and others, 1985; Huddlestun and Summerour, ments probably were deposited in less than 100 ft of water. 1996). In order to understand the stratigraphy in eastern The Santee Limestone is of late middle Eocene age. Fora- Georgia, detailed paleontological investigations were under- Bl B2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA taken. In 1991, we began our investigation of the Millers 82° 30' 81° 30' Pond core, which had been drilled recently by the GGS in northern Burke County (fig. 1). The USGS drilled two addi tional test holes—one in northern Screven County (Mill- haven test hole) and one in central Burke County (Girard test hole). The cores from these three test holes were designed to serve as the basis for stratigraphic correlation in 33° 30' - the area of Georgia adjacent to the SRS. Two other cores, drilled by the GGS, provide additional biostratigraphic information. This report synthesizes the biostratigraphic and paleoecologic investigation of these five cores collected from Burke and Screven Counties, Ga. The multidisciplinary paleontologic studies summa 33° rized here, and described in more detail in the individual chapters that follow, are based on the microfossils found in the cores. Palynomorphs and calcareous-walled microfossils were studied. Palynomorphs include pollen and spores from terrestrial plants, the cysts of marine dinoflagellates, and probable cysts of uncertain origin (acritarchs). Palyno 32° 30'- morphs are described in chapters by Frederiksen and others (this volume, chap. C) for Cretaceous sediments and by Edwards (this volume, chap. G) and Frederiksen (this vol Test hole site and informal name of site ume, chap. H) for Tertiary sediments. Calcareous microfos sils studied here include calcareous nannofossils (Bukry, this volume, chap. D) and ostracodes (Gohn, this volume, Figure 1. Index map showing the Savannah River Site and the chap. E) for Cretaceous material, and calcareous nannofos location of test holes in the study area. sils (Bybell, this volume, chap. F) and foraminifers (Gibson, this volume, chap. I) for Tertiary material. ments that were deposited on land (terrestrial sediments); Because few readers are familiar with every fossil however, pollen grains are easily transported by wind and group, we include a brief introduction to each. For the pur streams to the sea. Therefore, pollen grains are very useful pose of formal names of species and genera, palynomorphs for correlating terrestrial sediments and sedimentary rocks and calcareous nannofossils are classified by using the from one place to another, but they are also important for International Code of Botanical Nomenclature (Greuter and correlating sequences of terrestrial sediments with others, 1994); ostracodes and foraminifers are classified by sequences of marine sediments. using the International Code of Zoological Nomenclature The standard pollen zonation for the Upper Cretaceous (Ride and others, 1985). Under the botanical code, names of of the Gulf and Atlantic Coastal Plains was developed in a original authors and transferring authors are part of the for series of abstracts and papers by various authors and sum mal name of a species; under the zoological code, names of marized by Christopher (1982a). This zonation was based original authors are part of the formal name. Under both on material mainly from the Middle Atlantic States. The codes, the name of the original author is placed in parenthe only pollen zonation for the lower Tertiary of eastern North ses if the species has been reassigned. America was proposed by Frederiksen (1991, 1998) for the Paleocene. This zonation was based on material from the POLLEN eastern Gulf Coast, but it has also been applied to sections on the Atlantic Coastal Plain (Frederiksen, 1991, 1998). No Pollen grains are the sperm-carrying reproductive bod pollen zonation has been proposed for the Eocene and Oli- ies of higher plants; that is, gymnosperms (such as conifers gocene of eastern North America, but chronostratigraphic and cycads) and angiosperms (the flowering plants). Pollen ranges of the main pollen taxa in the Eocene and Oligocene grains are very small, typically between 0.01 and 0.1 milli of this region were displayed by Frederiksen (1979, 1980, meter (mm) in size. 1988). Pollen grains are produced mostly by plants living in land areas. The first gymnosperms evolved in the Devonian Period (about 385 million years ago), and the first DINOFLAGELLATES AND ACRITARCHS angiosperms evolved from gymnosperms early in the Creta ceous Period (about 140 million years ago). Pollen grains Dinoflagellates are single-celled organisms that live in are some of the most abundant fossils to be found in sedi- oceans, estuaries, lakes, and ponds. Here, they are consid- OVERVIEW OF THE BIOSTRATIGRAPHY AND PALEOECOLOGY OF SEDIMENTS FROM FIVE CORES, GEORGIA B3 ered to be plants because many of them are photosynthetic. plankton zone is designated by "NP" followed by a number. Some dinoflagellates are herbivores, carnivores, parasites, Calibration to the Cenozoic zonation of Bukry (1973, 1978) or symbionts. and Okada and Bukry (1980) also is provided. Many dinoflagellates have a complex life cycle that includes a resting stage. During this stage, the organism may live in a very durable capsule called a dinocyst. Nearly OSTRACODES all fossil dinoflagellates studied by paleontologists are cysts; however, the genera Alisogyrnnium and Dinogymnium Ostracodes are a group of fossil and modern, small, in the Cretaceous may be the covering from the motile bivalved crustaceans; modern species inhabit a wide variety stage. Nearly all dinocysts that are preserved in the fossil of aquatic environments. They are well represented in the record are from marine dinoflagellates. fossil record primarily by their hinged, smooth or orna Dinoflagellates form distinctive and rapidly evolving mented, calcified-chitinous valves and are common in fossils that may be found in marine rocks wherever a marine deposits of the Atlantic Coastal Plain. Typical Creta silt-sized component is present. There is, as yet, no widely ceous and Cenozoic forms in the coastal plain range in size accepted standard zonation for them. Important lowest and from 0.6 mm to 1.1 mm. highest occurrence datums are used to correlate locally and Ostracodes are mostly a benthic group. Accordingly, intercontinentally. The presence of fossil dinoflagellates can the compositions of ostracode assemblages, and the distri generally be used to infer marine deposition, and the abun butions and morphologies of individual taxa, are strongly dance of dinoflagellates from major taxonomic categories, influenced by environmental factors, including water depth, typically families such as the Peridiniaceae and Areoliger- turbidity, salinity, oxygen content, and food supply. As a aceae, may be used to infer additional paleoenvironmental result, ostracode assemblages tend to be useful in the paleo conditions. environmental analysis of sedimentary sections. They also Acritarchs are, by definition, palynomorphs of uncer are useful biostratigraphic indicators in local and regional tain origin. Two distinctive acritarchs are included with the studies where the effects of paleoenvironmental conditions dinoflagellates in the Tertiary study (Edwards, this volume, on species distributions are reasonably well known. The chap. G). ostracode interval zones of Hazel and Brouwers (1982; modified by Pitakpaivan and Hazel, 1994) are frequently used in biostratigraphic studies of ostracodes from Upper CALCAREOUS NANNOFOSSILS Cretaceous sediments in the Atlantic Coastal Plain.

Calcareous nannofossils are fossil remains of golden-brown, single-celled algae that live only in the FORAMINIFERS oceans. They are one of the primary organisms at the base of the food chain. These algae make tiny calcite platelets Foraminifers are similar to amoeboid organisms in cell inside their cells. These platelets are the calcareous nanno structure but differ in having granular rhizopodia and elon fossils that fall to the ocean bottom and become part of the gate pseudopodia that emerge from the cell body. Foramini clay-sized fraction in the sediment. Most calcareous nanno fers are covered with an organic test and typically have a fossils are formed by coccolithophorid algae and can also be wall composed of calcite or an agglomeration of mineral called coccoliths. grains embedded in the organic test. Foraminifers are com Calcareous nannofossils have been living in the posed of two primary groups: planktonic foraminifers world's oceans from the Triassic Period, and they have (marine floaters), and benthic foraminifers (sea-floor dwell evolved and changed rapidly and constantly over time. They ers). Fossils of both groups are included here. are extremely useful for dating marine sediments because Benthic foraminiferal morphologies are very diverse, existing zonations have a precision of 1 million to 4 million from simple single-chambered to multichambered, complex years or even less. forms with tests composed of calcite or mineral grains. In the last three decades, relatively stable standard bio- Benthic foraminifers occupy a wide range of marine envi stratigraphic zonations have been developed for calcareous ronments, from brackish estuaries to the deep ocean basins, nannofossils. A lowest or highest stratigraphic occurrence and occur at all latitudes. They can be used to infer the (FAD, first appearance datum; LAD, last appearance datum) salinity and water depths for sedimentary deposits and to is used to define the base and top of each zone. For the Cre recognize oxygen and productivity levels of environments. taceous, we use the biostratigraphic zonation of Planktonic foraminifers, which typically provide more pre Perch-Nielsen (1985), modified from Sissingh (1977), in cise age control than benthic species, occur in low numbers which each zone has a formal name and an informal abbre in the cores examined in this study; however, they are valu viation ("CC" followed by a number). For the Cenozoic, we able in the recognition of the upper lower Paleocene strata use the zonation of Martini (1971) in which each nanno- in the Millhaven core. As is typical in shallow-water depos- B4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA its, the few planktonic specimens recovered from the basement rock. A nearby hole, Millers Pond test well remaining samples consist mainly of juvenile individuals. 1, was logged for geophysical properties. • The McBean test hole (GGS-3757, Burke 5) was drilled by the GGS in 1991 in northern Burke County ACKNOWLEDGMENTS on the north shoulder of Collins Road 1.1 mi east of the intersection of Georgia Route 56 and Collins Road We thank U.S. Geological Survey colleagues John S. at lat 33°13'38" N., long 81°55'50" W. Surface eleva Clarke, W. Fred Falls, R. Parley Fleming, and David C. tion is 297 ft above sea level. The hole was cored to a Prowell, as well as Paul F. Huddlestun (Georgia Geologic depth of 327 ft and bottomed in the Upper Cretaceous Survey, Atlanta) and palynological consultant Joyce Steel Creek Formation. Lucas-Clark (Fremont, Calif.) for the sharing of data and ideas and the sometimes lively discussions that helped shape the ideas in this paper. Jonathan R. Bryan (Okaloosa- STRATIGRAPHIC FRAMEWORK Walton Community College, Niceville, Fla.) kindly looked at the larger foraminifers from the Millhaven core. We owe The stratigraphic framework of the coastal plain sec many thanks to Raymond A. Christopher (Clemson Univer tion in Screven and Burke Counties is discussed in detail by sity) for his willingness to review the entire volume. Falls and Prowell (this volume, chap. A). From oldest to youngest, the lithostratigraphic units that are considered are the Cretaceous Cape Fear Formation, Middendorf Forma MATERIAL AND METHODS tion, Black Creek Group, and Steel Creek Formation and the Tertiary Ellenton Formation, Snapp Formation, Fourmile This study is based on the paleontology in five cores in Branch Formation, Congaree Formation, Warley Hill For east-central Georgia (fig. 1). They are listed here in order mation, Santee Limestone, and Barnwell unit. In the Mid from the most basinward to the most onshore (updip). dendorf Formation and Black Creek Group, informal • The Millhaven test hole (33X048) was drilled by the subunits can be recognized lithostratigraphically in some U.S. Geological Survey (USGS) in 1991-92 in cores. We have used Falls and Prowell's lithostratigraphic northern Screven County on the Millhaven Plantation, framework as a starting point to discuss the biostratigraphy 2 miles (mi) northeast of Brier Creek and about 7 mi and paleoecology. west of the Savannah River at lat 32°53'25" N., long Figure 2 shows some of the terminology that has been 81°35'43" W. Surface elevation is 110 feet (ft) above used for lithostratigraphic units in the Atlantic and Gulf of sea level. This hole was cored to a depth of 1,452 ft Mexico Coastal Plains and their chronostratigraphic correla and bottomed in the Upper Cretaceous Cape Fear tions. In the Upper Cretaceous, we use the European stage Formation. boundaries summarized by Burnett and others (1992) and Gradstein and others (1995). The Campanian-Maastrichtian • The Girard test hole (32Y020) was drilled by the boundary position these authors use is stratigraphically USGS in 1992 in southern Burke County at the look higher (younger) than some previous interpretations of this out tower on Griffins Landing Road, 2 mi north of the boundary. town of Girard at lat 33°03'54" N., long 81°43'13" W. Surface elevation is 250 ft above sea level. This hole Important biostratigraphic and paleoecologic informa was cored to a depth of 1,385 ft and bottomed in tion from the three primary cores (Millhaven, Girard, and pre-Cretaceous red beds. Millers Pond) is given in graphic form in figures 3, 4, 5, 6, 7, and 8. • The Thompson Oak test hole (GGS-3794, TR92-6, Burke 12) was drilled by the Georgia Geologic Survey (GGS) in 1993 in northeastern Burke County, 21 mi BIOSTRATIGRAPHY AND south of Augusta just above the flood plain of the PALEOECOLOGY Savannah River at lat 33°10'42" N., long 81°47'10" W. Surface elevation is 240 ft above sea level. The hole was cored to a depth of 1,010.5 ft and bottomed in CAPE FEAR FORMATION gneissic basement rock. • The Millers Pond test hole (GGS-3758, Burke 2) was The Cape Fear Formation consists of gravels, sands, drilled by the GGS in 1991 in northern Burke County, silts, and clays that typically are arranged in fining-upward about 2 mi west of the Savannah River, 16 mi south of sequences. It was sampled only in the Millers Pond core. Augusta at lat 33°13'48" N., long 81°52'44" W. Sur Four clay layers were sampled, and two of these samples face elevation is 245 ft above sea level. The hole was yielded palynomorphs. The pollen present in the lower sam cored to a depth of 859 ft and bottomed in gneissic ple (847-852 ft) represents undifferentiated pollen Zone V OVERVIEW OF THE BIOSTRATIGRAPHY AND PALEOECOLOGY OF SEDIMENTS FROM FIVE CORES, GEORGIA B5

(Frederiksen and others, this volume, chap. C) of late Coni- Group in the Millhaven core was studied for calcareous nan- acian and Santonian age. The upper sample (827-832 ft) nofossils and ostracodes. represents the combined Complexiopollis exigua-Santala- Subunit 1 of the Black Creek Group is probably cites minor and Pseudoplicapollis longiannulata-Plicapollis mid-Campanian, pollen Zone CA-4 (Wolfe, 1976), in the incisa Zones but most likely belongs to the Complexiopollis Millhaven core (one sample, at 1,124.3-1,124.7 ft). Subunit exigua-Santalacites minor Zone (= Subzone V-A) of Chris 1 was not examined for pollen in the other cores (Frederik topher (1977, 1979, 1982a,b) of Coniacian age (Sohl and sen and others, this volume, chap. C). Owens, 1991). The absence of marine palynomorphs (dinoflagellates, acritarchs) and microforaminiferal linings The calcareous part of subunit 2 of the Black Creek in suggests a nonmarine environment of deposition. the Millhaven core (1,077-968 ft) is dated by calcareous nannofossils as late Campanian, calcareous nannofossil Zone CC 22, based on the co-occurrence of Quadrum trifi- MIDDENDORF FORMATION dum (Stradner) Prins & Perch-Nielsen and Reinhardtites anthophorus (Deflandre) Perch-Nielsen (Bukry, this vol The Middendorf Formation consists predominantly of ume, chap. D). The total range of the ostracode Haplo- moderately to poorly sorted, unlithified sand. It is subdi cytheridea sarectaensis Brown is limited to the upper part of vided into two subunits that each consist of a basal lag Zone CC 22 in the Millhaven core and in South Carolina deposit, sand, and interbedded and interlaminated clay and sections. Its highest occurrence can be used as a regional sand (Falls and Prowell, this volume, chap. A). Palyno marker that approximates the Campanian-Maastrichtian morphs from the Middendorf Formation were studied from boundary (Gohn, this volume, chap. E). the Millhaven, Girard, and Millers Pond cores (Frederiksen A distinctive dinoflagellate assemblage containing and others, this volume, chap. C). In the Millhaven core Palaeohystrichophora infusorioides Deflandre, Xenascus (1,212 ft, subunit 2), pollen taxa represent undifferentiated ceratioides (Deflandre) Lentin & Williams, Cordosphaerid- Zone V, which is of late Coniacian and Santonian age. Each ium fibrospinosum Davey & Williams, andAndalusiella spi- of two samples from the Girard core (1,138-1,139 ft, sub- cata (May) Lentin & Williams is found in and slightly unit 1, and 1,012.0-1,012.3 ft, subunit 2) contains a seem above subunit 2 in the Millhaven core (1,029.5-913.8 ft). ingly heterogeneous set of pollen taxa whose known This dinoflagellate assemblage is used to assign a late Cam occurrences are Coniacian to Santonian, Campanian, and panian age to correlative sections containing this assem Maastrichtian. The pollen flora of the Girard sample from blage in the Girard (867.7-738.6 ft) and Thompson Oak subunit 2 suggests a latest Santonian(?) or earliest Campa (505 ft) cores (Frederiksen and others, this volume, chap. nian age. C). The available data do not provide an unequivocal age for the Middendorf Formation. Two different ages may be Subunit 3 of the Black Creek Group in the Millhaven present, one representing undifferentiated pollen Zone V core (one sample, at 849.3-849.6 ft) is dated as late Campa and one slightly younger (perhaps correlative with the Shep nian by dinocysts based on the presence of Palaeohystri herd Grove Formation in South Carolina). chophora infusorioides Deflandre (Frederiksen and others, Rare dinocysts in the Middendorf Formation from the this volume, chap. C). Millhaven core (1,212 ft, subunit 2) suggest a marginal In the Millers Pond core, the Black Creek Group is not marine or very nearshore marine environment. The two differentiated into subunits. One sample from 578 ft con samples from the Girard core and the sample from the Mill tains pollen indicating a possible latest Santonian or earliest ers Pond core lack marine palynomorphs. Campanian age, or some poorly defined younger age. A sec ond sample from 517 ft contains pollen indicating an appar ent mid-Campanian age. BLACK CREEK GROUP In the Millhaven and Girard cores, subunit 1 of the The Black Creek Group consists of sands and clays. Black Creek Group yielded only nonmarine palynomorphs, Although it is not differentiated into component formations whereas subunits 2 and 3 yielded both marine and nonma in this study, Falls and Prowell (this volume, chap. A) rec rine palynomorphs. In the Millhaven core, part of subunit 2 ognize three distinct subunits in the two most downdip (bas- contains marine calcareous nannofossils and inner-neritic inward) cores. These subunits are recognized on the basis of ostracode assemblages. The two samples studied from the lag deposits and possible unconformities, but they cannot be Thompson Oak core were not assigned to a subunit but con related directly to named formations of the Black Creek tain marine palynomorphs. In the Millers Pond core, only Group that are recognized in South Carolina (Gohn, 1992). nonmarine palynomorphs were recovered in the Black The Black Creek Group was studied for palynomorphs in Creek Group (Frederiksen and others, this volume, chap. C). the Millhaven, Girard, Thompson Oak, and Millers Pond cores. The calcareous part of subunit 2 of the Black Creek Text continues on p. B14. B6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

SERIES EUROPEAN PROVINCIAL WESTERN ALABAMA1 subseries STAGE STAGE GEORGIA 2

Q_ Priabonian Jacksonian Limestone Clay ^^\_ Moodys Branch Fm. Moodys Branch Fm. CD c: Bartonian Gosport Sand CD •o Formation Formation Ypresian | Hatchetigbee/Bashi Fms. Hatchetigbee/Bashi Fms. Sabinian Tuscahoma Formation Tuscahoma Formation o3 Thanetian Nanafalia/Baker Hill Fms. Nanafalia/Baker Hill Fms. Q. Paleocene Q. Z> ^Jaheola Fm.> Selandian ':':'. : • Porters Creek Porters Creek Formation Midwayan Formation / Danian Clayton Formation Clayton Formation 1

Prairie Bluff Chalk Maastrichtian Providence Sand Navarroan Ripley Formation Ripley Formation

Demopolis Chalk Cusseta Sand Tayloran CO Campanian ^ o CD Mooreville Chalk Blufftown Formation O CO Austinian Eutaw Formation CD Santonian Eutaw Formation

O Coniacian McShan Formation Tuscaloosa Formation

CD Q. Turanian CL => Eaglefordian Tuscaloosa Formation Tuscaloosa Formation

Cenomanian /Woodbinian^^ '.''.• '. . ' '. : • • • : : ' Washitan (part)

Alabama column is based on Hazel (1990), Moshkovitz and Habib (1993), and Mancini and others (1996). "Western Georgia column is based on Prowell and others (1985) and Clarke and others (1994). Figure 2. Chart showing terminology that has been used for lithostratigraphic units in the eastern United States and our interpretations of their chronostratigraphic correlations. Mesozoic series and stages are from Burnett and others (1992) and Gradstein and others (1995); the Tertiary series, subseries, and stages are from Berggren and others (1995). OVERVIEW OF THE BIOSTRATIGRAPHY AND PALEOECOLOGY OF SEDIMENTS FROM FIVE CORES, GEORGIA B7

EASTEIFtN GEORGIA THIS STUDY SOUTH Lithologic Georgia Geologic NEW JERSEY 7 Units Survey Nomenclature 4 EASTERN GEORGIA 5 CAROLINA 6 §- \ Parkers Fe ry E8 2 Tobacco \ HarleyvilleF ms. Absecon Inlet Fm. Barnwell Barnwell = Road Sand / (Cooper Group) E7 Group unit 1 Dry Branch V £ Clinchfield ) E6

Santee Tinker \ s t Q. Shark River E5 Lisbon Formation Formation / Formatjon O Limestone O Formation ro E4 Still Branch Sand Warley Hill Formation Warley Hill Fm\ S ——— _Q 03 E3 TO Congaree Congaree Formation Huber / Congaree \ ro Formation Fm. \ Formation / 6 E2 Fourmile Branch Formation Manasquan E1 Fourmile Branch Fm.^shbume Fm- Formation Snapp Formation Snapp Formation / ^ P2 / Snapp Formation ______-Eilenion f grmajjpn ______MingoBlackGroup Vincentown LangSyne \ feltunrg Formation Ellenton Formation Formation / \ Formation ——————(Ellenton y ————— P1 Black Mingo Hornerstown Formation Ellenton Formation Sawdust \ Fm. ( Rhems Landing Fm. ) \ _ Formation (undifferentiated) / / Tinton Formation Steel Creek / Peedee Red Bank Formation UK6 Steel Creek Steel Creek Fm. Formation Formation / Formation Navasink Formation UK5 n , , Donoho Creek Fm. Mt. Laurel -Wenonah Fm. Black Creek Black UK4 Creek Bladen Formation Marshalltown Formation Gaillard / Black Group C rni n Coachman Formation Englishtown Formation Fm. ( Creek " Cane Acre Formation Woodbury Clay \ Fm. Caddin Formation Merchantville Fm. UK3 Shepherd Grove Fm. unnamed marine beds Middendorf Formation UK2 Pio Mono") Unnamed Middendorf Formation Fm. > Sand Magothy Formation UK1 Cape Fear Formation Cape Fear Formation Raritan Formation

Cape Fear Clubhouse Formation Formation B'assRive^Raritan Fm. /Formation Beech Hill Formation 'Lithologic unit column for eastern Georgia is based on Prowell and others (1985). 4Column of Georgia Geologic Survey nomenclature for eastern Georgia is based on Huddlestun and Summerour (1996). 5The column of names for this study of eastern Georgia shows separate entries for the Fourmile Branch Formation, the Congaree Formation, and the Warley Hill Formation. In chapter A, these three formations are combined into one unit as all three formations are not consistently present in the five cores studied. 6South Carolina column is based on Van Nieuwenhuise and Colquhoun (1982), Frederiksen (1991), Gohn (1992), Fallaw and Price (1995), Self-Trail and Gohn (1996), and Edwards and others (1997). 7New Jersey column is based on Owens and others (1970, 1988), Litwin and others (1993), Self-Trail and Bybell (1995), Kennedy and others (1995), and Browning and others (1997). Figure 2. Continued. o Nanno- Gamma ray g Single-point Geologic Dinocyst Foraminiferal o resistance (ohms) fossil Pollen zone (API units) unit zone datums indicators 50 150 100 200

late Eocene or early Oligocene larger forams 100 - Barnwell 21? unit 0-100 ft LLJ 19-21 LLJ

200 - 19/20 , C. funiculatum LU P. laticinctum C. variabilis B. baculata 0-100 ft DC ID CO Q 300 - > Santee 17 P. goniferum 0-100 ft Limestone _/ C. cantharellus 1100-200 ft

LU 15-17 CO 400 - 0-100 ft Fourmile ~^ P. favatum Q_ Branch/ P. goniferum LU I 1 15 A. diktyoplokus approx. 100ft Q Congaree/ G. cf. G.? vicina J4i15_ Warley Hill -\ T, cf. T, galatea approx. 300 ft o unit 14 _/ P. favatum, T. cf. T. approx. 100ft 500 - galatea Snapp Formation F. annetorpense, ^ P. pyrophorum low oxygen Caryapollenites prodromus Zone Phelodinium sp. of about 100 ft or less 600 - Ellenton Edwards (1989) Formation -f Andallusiella sp. less than 200 ft aff. A. polymorpha C. cornuta early Paleocene, P1 EXPLANATION Massive Clayey Limestone Sandy Marl ZE-I^- Laminated Sand ^>^ limestone clay clay sand

Figure 3. The stratigraphic and paleontologic summary of the Tertiary part of the Millhaven core. The lithology is from Clarke and others (1996), and the lithostratigraphy and geophysical logs are from Falls and Prowell (this volume, chap. A). Paleontologic data are from chapters F (nannofossil column), G (dinocyst column), H (pollen column), and I (foraminiferal indicators column). API, American Petroleum Institute. LITHOLOGY Nannofossil Ostracode assemblage Gamma ray Single-point SERIES Dinocyst Geologic STAGE zone and Pollen zone and inferred O (API units) resistance (ohms) datums unit datums paleoenvironment m 50 150 100 200 i i i 642 "j^~ j_ . __ .

700 - o Maastrichtian f Steel Creek Formation j— -^— - • —— Most likely ^T Maastrichtian o 800 - ? C/5 7EI-EZ r S. delitiense H SL, — / —— —r- '

LUtn P. infusorioides u. subunit3 LU"- 900 - \ O (T^^ assemblage includes P. infusorioides: A. spicata, UPPERCRETACEOUS Campanian assemblage 32 Group O r (t lithostratigraphy and geophysical logs are from Falls and Prowell (this volume, chap. A). Paleontologic data are from chapters C (pollen and dinocyst columns), D (nannofossil column), and E (ostracode column). API, American Petroleum Institute. td to o SUBSERIES Nanno- Gamma ray LITHOLOGY Single-point SERIES Dinocyst Geologic fossil Pollen zone (API units) resistance (ohms) unit datums zone 50 150 1 00 200 i i i

9 9 — — ^ LU LLJ 100 - Jr • i' i • Barnwell ^t^_^ *[ ' i • i • unit LLJ O ^^"^f — /— ~2 (D DC 200 - Q. R. peforatum, D / • i • i \ J • i- i - i Fourmile P. favatum CO ^ NP15 g5 Branch/ .P. favatum, — ' G. cf. G.I vicina Q_ v_ 0 Congaree/ GOn LU 4 NP 11-14 ^ ^ Warley Hill _ > H. tenuispinosum Q 400 - £ i "- ™ unit ^^=- — — t^~ w ^^ 9 9 -^_ Snapp ~i~- LU Formation Z j LU ^^^~ ^^ O /M ^ * ——. D. californicum, 500 ~ O ~ NP !>8 ~ I I I Ellenton LU ^j^^_ ^^^ =— mixed assemblages ^^* Formation NP1-4 ^rfi^ DL

:OUNTIES,GE EXPLANATION 1 1 - i imQotrtr,o 'J ; i .• ' Sandy -i . i . i- .. — — Massive ———— L aminateri . « —- — - Clavev -rV^. Limestone ^L^ |jmfistyone :——— : Ma .nd • ^'«ycy rl nlflyj ————— rlfluy • • • • sand

Figure 5. The stratigraphic and paleontologic summary of the Tertiary part of the Girard core. The lithology is from Leeth and others (1996), and the lithostratigraphy and geophysical logs are from Falls and Prowell (this volume, chap. A). Nannofossil zones are inferred from palynological evidence. Other paleontologic data are from chapters G (dinocyst column) and H (pollen column). API, American Petroleum Institute. Gamma ray Single-point O < (API units) resistance (ohms) w 50 150 542 I Steel Creek o 600 - Formation ^fl wa w o 700 - on H

Zone CA-4 assemblage or CA-5 includes P. infusorioides O Black Creek A. spicata, X. - 800 - Group ceratioides, C. fibmspinosum, 5XI C. pannuceum a

lowest marine palynomorphs 900 - 5 highest § 1000 - Santonian O or lowest Campanian o Middendorf o Formation 1100 - c/a S 1200 - § H c/a Cape Fear Formation o 1300 - 2 w n 1375 o EXPLANATION pow Laminated clay i^ Clayey sand §O Figure 6. The stratigraphic and paleontologic summary of the Cretaceous part of the Girard core. The lithology is from o Leeth and others (1996), and the lithostratigraphy and geophysical logs are from Falls and Prowell (this volume, chap. A). > Nannofossil Zone CC 22 is inferred from palynological evidence. Other paleontologic data are from chapter C. API, American Petroleum Institute. bd fo

O w o r o o O SUBSERIES Nanno Gamma ray Single-point Geologic SERIES Dinocyst Foraminiferal 3 fossil Pollen zone o (API units) 0 resistance (ohms) unit datums indicators "0 1- zone > LU 50 150 175 190 LU _l w i i \ o J2==^——— Barnwell £ LU CD J^—— " Q. o O unit Q. 3 o W EOCENE Middle Eocene, o •1 • 1- 1- 100 - 5- . • 1 • ^ Santee ~ less than 1 00 ft (fi 1 i. r i- CU • . i • <_ Limestone T3 -NP 16-21 —^ P. goniferum _ Middle Eocene, Q ± -\ • \ • T3 less than 100ft • 1 • /Fourmile Branch/ ^ C. cantharellus • 1 • 1 • NP17* — £ P. goniferum - less than 100ft r Congaree/ __/P. favatum, T. cf. w ^^ IE- ^ NP14* T. galatea n \ Warley Hill unit £ < _ cu 200 - Snapp PALEOCENE CL LU CL CD > Formation => 3, -NP4-5* _ . single occurrence "s" Ellenton -NP3-4* \ 1. viborgense Q_ T — upper part, Pseudoplica- LU Formation o pollis serenus Zone C. cornuta Q 284 f nGO & EXPLANAT ON m •J | i |-i • bandy I aminated < Massive clay Sand m i- i- i limfistone — — c lay 2: > z; Figure 7. The stratigraphic and paleontologic summary of the Tertiary part of the Millers Pond core. The lithology is from Clarke and others (1994), and the lithostratigraphy and o Dd geophysical logs are from Falls and Prowell (this volume, chap. A). Nannofossil zone in bold is based on observed calcareous nannofossils (chapter F); nannofossils zones with an asterisk are inferred from palynological evidence (chapters G and H). Other paleontologic data are from chapters G (dinocyst column), H (pollen column), and I (foraminiferal indicators column). API, American Petroleum Institute. 8

c/a O O Q > O LJJ O Gamma ray 3 Single-point Geologic LJJ O o DC Pollen zone (API units) resistance (ohms) unit LJJ 50 150 175 190 284 Steel Creek 300 H Formation H W W O &o I- H LLJ LJJ 400 - LL H Black Creek O Group c LJJ 'cCO O ffi < CO LJ_ Q. DC 500 - o LJJ CO — Zone CA-4 or CA-5 (?) o o O Q Z fLJJ £ < DC O n 600 - DC o LJJ Q_ 5 LJJ Q_ 00 Middendorf => 9 X Formation O LJJ Q 700 -

c 'oCO 800 - Cape Fear 'cCO § Formation Probably Complexiopollis exigua- oo Santalacites minor Zone 852 n o EXPLANATION on Sand .—• —': Clayey sand O W O Figure 8. The stratigraphic and paleontologic summary of the Cretaceous part of the Millers Pond core. The lithology is from Clarke and others (1994), and the lithostratigraphy and geophysical logs are from Falls and Prowell (this volume, chap. A). The pollen data are from chapter C. API, American Petroleum Institute. B14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

STEEL CREEK FORMATION Although calcareous nannofossil Zone NP 4 includes both early and late Paleocene time, dinocysts and planktonic for The Steel Creek Formation consists of multiple fining- aminifers indicate that only the early Paleocene part of the upward sequences of gravel, sand, and clay, in which many zone is present in this core. Two samples from the Girard of the clay beds are stained with iron oxide (Falls and Prow- core were examined for calcareous nannofossils; both ell, this volume, chap. A). The formation was sampled proved barren. unproductively in the Millers Pond core and was not sam A distinctive early Paleocene dinocyst assemblage that pled in the Girard and Thompson Oak cores. Ten samples includes Carpatella cornuta Grigorovich, Spinidinium pul- from the Millhaven core were examined for palynomorphs chrum (Benson) Lentin & Williams, Tectatodinium rugula- (Frederiksen and others, this volume, chap. C). tum (Hansen) McMinn, and Tenua sp. cf T. formosa of The lowest Steel Creek samples contain pollen taxa Kurita and Mclntyre (1995) is present in the lowest Ellenton that were not found to range below this formation in the in the Millhaven core (one sample at 639.5 ft), the Girard Millhaven core. A new species, Momipites n. sp. 1, is known core (521.2-517.9 ft, questionably to 514 ft), and the Mill only from the Maastrichtian. These samples are correlative ers Pond core (one sample at 252-257 ft). In the Millhaven with middle or late Maastrichtian units in New Jersey, or core, the late Paleocene dinoflagellate assemblage includes perhaps the unconformity below them. The sample at Palaeoperidinium pyrophorum (Ehrenberg) Sarjeant and 830.3-830.5 ft contains a rather sparse dinoflagellate Fibradinium annetorpense Morgenroth in the highest sam assemblage that includes Spongodinium delitiense (Ehren- ple (571ft). berg) Deflandre (lowest occurrence is in the uppermost Early Paleocene (Danian) pollen was identified in the Campanian in New Jersey). Samples at 768.8-769.0 and Millers Pond core in the lowest Tertiary sample (252-257 733.2-733.3 ft contain long-ranging Cretaceous forms of ft). In the Girard core, the pollen assemblage in one of the pollen, and a sample at 680.8-681.0 ft is barren of palyno Ellenton samples (521.0-521.2 ft) consists of species that morphs and contains only plant debris. Samples from the normally do not occur together. Although alternative inter correlative interval (based on geophysical logs) in the C-10 pretations are possible, contamination from above into core (Allendale County, S.C.) yielded nonmarine assem lower Paleocene material is most likely. In the Thompson blages dated as Maastrichtian (Joyce Clark, 1989, written Oak core, pollen at 302 ft depth could be either late early or commun. to the South Carolina Water Resources Commis early late Paleocene. Late Paleocene pollen was found in six sion). Thus, a combination of pollen and dinoflagellate data samples in the Millhaven core (620.8-571.0 ft) and in the suggests that the Black Creek Group-Steel Creek Formation Thompson Oak core (281 ft). In the McBean core, the boundary approximates the Campanian-Maastrichtian Ellenton was barren of pollen (Frederiksen, this volume, boundary in the Millhaven core. chap. H). The lowest Steel Creek sample in the Millhaven core In the Ellenton of the Millhaven core, five intervals contains a few marine dinoflagellates. No marine fossils with differing foraminiferal assemblages are present: (1) a were recovered higher in the unit. highly altered, low-diversity assemblage of early, but not earliest, Paleocene age, planktonic foraminiferal Zone PI (636.8 ft); (2) an assemblage containing apparent mixing of ELLENTON FORMATION specimens from lower Paleocene beds with early late Pale ocene specimens (631.3 ft); (3) an assemblage suggesting The Ellenton Formation consists of sands and clays normal productivity and oxygen levels with a probable that are partly glauconitic and calcareous in the Millhaven water depth range of 100 to 200 ft (628.7 ft); (4) an assem core (most basinward) and lignitic in the Millers Pond core blage suggestive of water depths of less than 100 ft but hav (Falls and Prowell, this volume, chap. A). This unit was ing high-productivity or low-oxygen conditions or both studied for calcareous nannofossils, foraminifers, and (621.2-599.1 ft); and (5) an assemblage suggestive of water marine and nonmarine palynomorphs in the Millhaven core. depths of less than 100 ft with normal marine oxygen condi It was studied for palynomorphs in the Girard, Thompson tions (593.7-581 ft). Age-diagnostic planktonic foramini Oak, and Millers Pond cores. A very thin lower Paleocene fers are present only in the lowest part of the Ellenton, but (Danian) section is present in at least three of the Georgia benthic species and immature planktonic species are present cores. Most of the Ellenton is early late Paleocene (Selan- throughout (Gibson, this volume, chap. I). dian). Two samples in the Millhaven core are middle late Paleocene (Thanetian). In the Millhaven core, the Ellenton yields three distinct SNAPP FORMATION calcareous nannofossil zones: NP 4 (early Paleocene, 639.6-635.4 ft), NP 5 (early part of the late Paleocene, The Snapp Formation consists of a lower sand-domi 631.3-579.2 ft), and NP 8 (middle part of the late Pale nated part and an upper clay-dominated part. The formation ocene, 578.0-577.2 ft) (Bybell, this volume, chap. F). was studied for palynomorphs in the Millhaven and OVERVIEW OF THE BIOSTRATIGRAPHY AND PALEOECOLOGY OF SEDIMENTS FROM FIVE CORES, GEORGIA B15

McBean cores. No samples from the Snapp Formation were Formation in the studied cores (Edwards, this volume, chap. taken from the Millers Pond and Girard cores, and the for G). Both assemblages contain Pentadinium favatum mation is absent from the Thompson Oak core. In the Edwards. One assemblage, which contains Turbiosphaera McBean core, where the Snapp Formation consists only of cf. 7. galatea Eaton, is found in the lower part of the sand with no overlying kaolin, nonmarine palynomorphs are Congaree Formation in the Millhaven core (498.5-473.5 ft), present (Frederiksen, this volume, chap. H). The overlap the Thompson Oak core (231.5 ft), and the Millers Pond ping ranges of pollen taxa in the one productive sample (254 (165 ft) core. The dinocysts in this assemblage appear to be ft) indicate an age no older than earliest late Paleocene and correlative with those in the upper part of the Tallahatta no younger than middle late Paleocene age (Selandian or Formation in Alabama and unit E3 of Prowell and others Thanetian). (1985) in Georgia. A second assemblage, which contains A single Snapp sample in the Millhaven core (564-565 Glaphyrocysta cf. G.? vicina (Eaton) Stover & Evitt, is ft) yielded rare dinocyst fragments that are not age diagnos found in the Millhaven core at 466 ft and also in the Girard tic but indicate at least marginally marine conditions (362.3-327.3 ft) and Thompson Oak (194-183.5 ft) cores. (Edwards, this volume, chap. G). This assemblage is correlative with that from the lower part of the Lisbon Formation in Alabama. Pollen studies of the Congaree yielded generally broad FOURMILE BRANCH FORMATION age possibilities: early or middle Eocene in the Millhaven The Fourmile Branch Formation, a medium to coarse core and correlative with calcareous nannofossil Zone NP sand, was recognized only in the Girard and Thompson Oak 12 to early NP 16 in the Thompson Oak core (Frederiksen, cores (Falls and Prowell, this volume, chap. A). It was this volume, chap. H). examined for palynomorphs in these cores. Foraminifers from the Congaree Formation in the Mill- A distinctive dinocyst assemblage, containing both haven core indicate a middle Eocene age and generally indi Hafniasphaera goodmanii Edwards and primitive forms of cate a water depth of approximately 100 ft. A single sample Pentadinium favatum Edwards, was found in the Fourmile at 481 ft indicates much deeper water, approximately 300 ft Branch Formation in the Thompson Oak core. Homotryb- (Gibson, this volume, chap. I). lium abbreviatum Eaton is also present. These species are also found in the lower part of the Tallahatta Formation in Alabama and thus suggest correlation with lower Eocene WARLEY HILL FORMATION calcareous nannofossil Zones NP 12 or NP 13. Sediments in the Fourmile Branch Formation in the Girard core contain The Warley Hill Formation, a sandy limestone, was Dracodinium varielongitudum (Williams & Downie) Costa recognized only in the Millhaven core (Falls and Prowell, & Downie and Homotryblium tenuispinosum Davey & Will this volume, chap. A). It was studied for calcareous nanno iams and are probably of early Eocene age as well fossils, foraminifers, and palynomorphs. (Edwards, this volume, chap. G). Most samples from the Warley Hill Formation in the Pollen from the Fourmile Branch Formation indicates Millhaven core (458.1-413.0 ft) are assigned to the middle an early Eocene age, or possibly early middle Eocene, in the Eocene calcareous nannofossil Zone NP 15. The lowest Girard core. The dinocysts present indicate that sediments sample (462 ft) could be either NP 14 or NP 15, and the from the Fourmile Branch Formation are marine. highest sample (404 ft) could be either NP 15 or 16. Preser vation in all samples is fair or poor. The dinocyst assemblage from the Millhaven samples CONGAREE FORMATION at 442 and 413 ft contains both Pentadinium goniferum The Congaree Formation consists of quartz sand, marl, Edwards and P. favatum Edwards. These two species are and limestone. Samples from the Congaree Formation were found together only in sediments from a narrow interval in studied for calcareous nannofossils, foraminifers, and the middle Eocene that is probably correlative with the mid palynomorphs from the Millhaven core and for dle part of the Lisbon Formation in Mississippi and with an palynomorphs in the Girard, Thompson Oak, Millers Pond, unconformity or condensed interval within the Lisbon For and McBean cores. mation in Alabama (Edwards, this volume, chap. G). These In the Millhaven core, the Congaree Formation yields species were observed to overlap in part of unit E4 of Prow calcareous nannofossils that are placed in Zone NP 14 ell and others (1985). (early and middle Eocene, 497.4-473.5 ft); the uppermost Foraminifers from samples at 455 and 426.5 ft in the sample (465.5 ft) could be either NP 14 or NP 15 (middle Millhaven core were probably deposited in 100-ft water Eocene) (Bybell, this volume, chap. F). depth or slightly deeper, whereas those in samples at 413 Two distinctive dinocyst assemblages, both of early and 404 ft in the core were probably deposited in less than middle Eocene age, can be recognized in the Congaree 100 ft of water (Gibson, this volume, chap. I). B16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

SANTEE LIMESTONE In the Millhaven core, nannofossil samples from 225.9 to 168.5 ft are late Eocene (Zone NP 19/20). Samples from The Santee Limestone consists primarily of limestone 118.0 to 95.0 ft are questionably dated as Zone NP 21 (latest and unlithified carbonate sediments with a few beds of cal Eocene or earliest Oligocene). careous sand and clay (Falls and Prowell, this volume, chap. Dinocysts from Millhaven samples at 216.5, 210, and A). Samples from the Santee were studied for calcareous 205 ft are most likely of late Eocene age, and the two upper nannofossils, foraminifers, and palynomorphs from the samples suggest correlation with the upper Eocene Yazoo Millhaven and Millers Pond cores and for palynomorphs Clay in Alabama and the Harleyville and Parkers Ferry For from the Girard, Thompson Oak, and McBean cores. mations in South Carolina. Samples at 195, 118, and 105 ft In the Millhaven core, the samples from 400.0-370.9 ft were barren of dinocysts. In the Girard core, the sample at have poorly preserved calcareous nannofossil assemblages 211.1-211.3 ft contains dinocyst species that suggest a late and could be in Zones NP 15, 16, or 17 (middle Eocene). Eocene age. The sample at 146.7 ft contains a very sparse Beginning at 368.0 ft and continuing to the top of the forma and nondiagnostic dinocyst assemblage, and samples at 104 tion, calcareous nannofossils indicate late middle Eocene and 64 ft were barren of dinocysts. Zone NP 17. The Santee Limestone in the Millers Pond core Most samples from the Barnwell unit yielded marine contains Eocene calcareous nannofossils that are not very calcareous microfossils and marine palynomorphs. The for- age diagnostic. The Santee Limestone was not studied for aminiferal assemblage suggests shallow-marine environ calcareous nannofossils in the other three cores because of ments, probably in the deeper portion of the 0- to 100-ft the anticipated poor assemblages (Bybell, this volume, depth interval. chap. F). In the Millhaven core, dinocyst samples have poor recovery in the lower part of the Santee Limestone but have SUMMARY AND IMPLICATIONS abundant and distinctive assemblages above 346 ft that are typical of the late middle Eocene, correlative with the upper The Cape Fear Formation, where studied, is of proba part of the Lisbon Formation in Alabama and perhaps the ble Coniacian age and is nonmarine. Gosport Formation. In the Girard, Thompson Oak, Millers The available data do not provide an unequivocal age Pond and McBean cores, the Santee Limestone contains late for the Middendorf Formation. Two different ages may be middle Eocene dinocyst assemblages similar to those found present, one representing undifferentiated pollen Zone V in the Millhaven core (Edwards, this volume, chap. G). (late Coniacian and Santonian) and one slightly younger Foraminifera from the Millhaven and Millers Pond (latest Santonian(?) and early Campanian, perhaps cores indicate a middle Eocene age, and most samples con correlative with the Shepherd Grove Formation in South tain the distinctive benthic species Cibicides westi Howe Carolina). The possibility of similar lithofacies representing (Gibson, this volume, chap. I). different ages should be considered and investigated further. The Santee Limestone contains only poorly dated pol Most of the Middendorf Formation is nonmarine. Rare len (Frederiksen, this volume, chap. H). dinocysts in a single sample from the Millhaven core (1,212 ft, subunit 2) suggest a marginal marine or very nearshore Foraminifers indicate paleo-water depths of 100 to 200 marine environment. ft in the lower part of the Santee Limestone and less than 100 ft in its upper part in the Millhaven core and water The Black Creek Group is dated as Campanian. It is depths of less than 100 ft in the Millers Pond core (Gibson, nonmarine in its lower part (subunit 1). In all but the most this volume, chap. I). updip core, the Black Creek Group includes marine fossils in its upper part (subunits 2 and 3). Subunit 2 contains ostracodes correlative with those in the Donoho Creek Forma BARNWELL UNIT tion, the highest formation in the Black Creek Group in central South Carolina (Gohn, 1992). Subunit 3 may repre The Barn well unit is a mixed lithologic sequence of sent deposition in Georgia that has no counterpart in central sandy limestone, marl, clay, and sand. It is treated as a unit, South Carolina. although unconformities can be recognized within it (Falls The Steel Creek Formation is Maastrichtian in the and Prowell, this volume, chap. A). Sediments of the unit Millhaven core. It contains a few marine dinoflagellate cysts are poorly fossiliferous. The unit was sampled in the Mill- near its base; no marine fossils were recovered higher in the haven core for calcareous nannofossils and palynomorphs unit. and in the Girard core for palynomorphs only. Sediments of The placement of the Cretaceous-Tertiary boundary in the Barn well unit from the Thompson Oak, Millers Pond, all cores is, of necessity, based on the lithostratigraphy and McBean cores either were not sampled in this study or (Falls and Prowell, this volume, chap. A). Thick undated did not contain palynomorphs. intervals are found between the Maastrichtian of the Steel OVERVIEW OF THE BIOSTRATIGRAPHY AND PALEOECOLOGY OF SEDIMENTS FROM FIVE CORES, GEORGIA B17

Creek Formation or Campanian of the Black Creek Group Sediments of the Barnwell unit are poorly fossilifer- and the Danian of the Ellenton Formation. ous. Where they can be dated, they are late Eocene to ques A very thin lower Paleocene (Danian) section is tionably early Oligocene. Most samples are shallow marine. present at the base of the Ellenton Formation in at least three cores. Most of the Ellenton Formation is early late Pale ocene (Selandian). Two samples in the Millhaven core are REFERENCES CITED middle late Paleocene (Thanetian). The oldest Paleocene Berggren, W.A., Kent, D.V, Obradovich, J.D., and Swisher, C.C., material contains a significant component of planktonic for- HI, 1992, Towards a revised Paleogene geochronology, in aminifers and, thus, represents deeper water deposition than Prothero, D.R., and Berggren, W.A., eds., Eocene-Oligocene the remainder of the Ellenton Formation. climatic and biotic evolution: Princeton, N.J., Princeton Uni The Snapp Formation is present in varying thicknesses versity Press, p. 29-45. in four of the five cores and is dated as late Paleocene Berggren, W.A., Kent, D.V, Swisher, C.C., HI, and Aubry, M.-P, (Selandian or Thanetian). It is mostly nonmarine. A single 1995, A revised Cenozoic geochronology and chronostratig- sample from the Millhaven core yielded dinocyst fragments raphy, in Berggren, W.A., Kent, D.V, Aubry, M.-P, and Hard- enbol, Jan, eds., Geochronology, time scales and global that indicate marginally marine conditions. stratigraphic correlation: SEPM (Society for Sedimentary The Snapp Formation is conspicuously absent from the Geology) Special Publication 54, p. 129-212. Thompson Oak core, and the upper kaolinitic part is not Browning, J.V, Miller, K.G., and Bybell, L.M., 1997, Upper present in the McBean core. Because the Snapp Formation Eocene sequence stratigraphy and the Absecon Inlet Forma is present in the most updip cores, it was probably also tion, New Jersey Coastal Plain, in Miller, K.G., and Snyder, present in the Thompson Oak area originally but subse S.W., eds., Proceedings of the Ocean Drilling Program, Scien quently removed. Faulting is well documented in South tific Results, v. 150X, p. 243-266. Carolina (Snipes and others, 1993), but the Thompson Oak Bukry, David, 1973, Low-latitude coccolith biostratigraphic zona- core is located on the downthrown side of the Pen Branch tion, in Edgar, N.T., Saunders, J.B., Bolli, H.M., Boyce, R.E., Broecker, W.S., Donnelly, T.W., Gieskes, J.M., Hay, W.W., fault (Huddlestun and Summerour, 1996). We suggest that Horowitz, R.M., Maurrasse, Florentin, Perez Nieto, Hernan, erosion by a predecessor to the Savannah River should be Prell, Warren, Premoli Silva, Isabella, Riedel, W.R., Schnei- considered and investigated further. dermann, Nahum, Waterman, L.S., Kaneps, A.G., Herring, The Fourmile Branch Formation is early Eocene and is J.R. (ed.), Initial reports of the Deep Sea Drilling Project, v. only found in the Thompson Oak and Girard cores. Erosion 15: Washington, D.C., U.S. Government Printing Office, p. of the underlying Snapp Formation in the Thompson Oak 685-703. core may have facilitated preservation of these early Eocene ————1978, Biostratigraphy of Cenozoic marine sediments by sediments. The presence of dinocysts indicates that sedi calcareous nannofossils: Micropaleontology, v. 24, p. 44-60. ments from the Fourmile Branch Formation are marine. Burnett, J.A., Hancock, J.M., Kennedy, W.J., and Lord, A.R., 1992, Macrofossil, planktonic foraminiferal and nannofossil The Congaree Formation is of middle Eocene age. It zonation at the Campanian/Maastrichtian boundary: Newslet contains two recognizable dinocyst assemblages that are ters on Stratigraphy, v. 27, no. 3, p. 157-172. roughly equivalent to those from the upper part of the Talla- Christopher, R.A., 1977, The stratigraphic distribution of Nor- hatta Formation and from the lower part of the Lisbon For mapolles and triporate pollen in Zones IV, V and VII of the mation of the Gulf Coast. Foraminifers from the Congaree Raritan and Magothy Formations (Upper Cretaceous) of New Formation in the Millhaven core generally indicate a water Jersey [abs.]: American Association of Stratigraphic Palynol- depth of approximately 100 ft; a single sample at 481 ft ogists, 10th Annual Meeting, Abstracts with Program, p. 7-8. indicates much deeper water, approximately 300 ft. Reprinted 1979 in Palynology, v. 3, p. 281. ————1979, Normapolles and triporate pollen assemblages from The Warley Hill Formation, a marine unit of middle the Raritan and Magothy Formations (Upper Cretaceous) of Eocene age, is recognized only in the Millhaven core. Fora New Jersey: Palynology, v. 3, p. 73-121, pis. 1-9. minifers from samples at 455 and 426.5 ft in the Millhaven ————1982a, Palynostratigraphy of the basal Cretaceous units of core were probably deposited in 100-ft water depth or the eastern Gulf and southern Atlantic Coastal Plains, in slightly deeper; whereas those from higher samples were Arden, D.D., Beck, B.F., and Morrow, Eleanore, eds., Pro probably deposited in less than 100 ft of water. ceedings; Second symposium on the geology of the southeast ern coastal plain: Georgia Geologic Survey Information The Santee Limestone is of late middle Eocene age. It Circular 53, p. 10-23, pis. 1-3. contains calcareous fossils even in the most updip cores. -1982b. The occurrence of the Complexipollis-AtlantopoUis Not surprisingly, the paleo-water depth increases basinward. Zone (palynomorphs) in the Eagle Ford Group (Upper Creta In the Millers Pond core, inferred depths are less than 100 ft ceous) of Texas: Journal of Paleontology, v. 56, no. 2, p. 525- throughout the unit; in the Millhaven core, inferred depths 541, pi. 1. range from 100 to 200 ft in the lower part of the formation Clarke, J.S., Falls, W.F., Edwards, L.E., [Bukry, David,] Frederik- and are less than 100 ft near the top. sen, N.O., Bybell, L.M., Gibson, T.G., Gohn, G.S., and Flem- B18 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

ing, Parley, 1996, Hydrogeologic data and aquifer Huddlestun, P.P., and Summerour, J.H., 1996, The lithostrati- interconnection in a multi-aquifer system in coastal plain sed graphic framework of the uppermost Cretaceous and lower iments near Millhaven, Screven County, Georgia, 1991—95: Tertiary of eastern Burke County, Georgia: Georgia Geologic Georgia Geologic Survey Information Circular 99, 43 p., 1 pi. Survey Bulletin 127, 94 p. in pocket. Kennedy, W.J., Johnson, R.O., and Cobban, W.A., 1995, Upper Clarke, J.S., Falls, W.F., Edwards, L.E., Frederiksen, N.O., Bybell, Cretaceous ammonite faunas of New Jersey, in Baker, J.E.B., L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, ed., Contributions to the paleontology of New Jersey: Geolog hydrologic and water-quality data for a multi-aquifer system ical Association of New Jersey Contribution Proceedings, v. in coastal plain sediments near Millers Pond, Burke County, 12, p. 24-55. Georgia, 1992-93: Georgia Geologic Survey Information Cir Kurita, Hiroshi, and Mclntyre, D.J., 1995, Paleocene dinoflagel- cular 96, 34 p., 1 pi. in pocket. lates from the Turtle Mountain Formation, southwestern Man Edwards, L.E., Bybell, L.M., Gohn, G.S., and Frederiksen, N.O., itoba, Canada: Palynology, v. 19, p. 119-136. 1997, Paleontology and physical stratigraphy of the Leeth, D.C., Falls, W.P, Edwards, L.E., Frederiksen, N.O., and USGS-Pregnall No. 1 core (DOR-208), Dorchester County, Fleming, R.P, 1996, Geologic, hydrologic, and water-chem South Carolina: U.S. Geological Survey Open-File Report istry data for a multi-aquifer system in coastal plain sediments 97-145, 35 p. near Girard, Burke County, Georgia, 1992-95: Georgia Geo Fallaw, W.C., and Price, Van, 1995, Stratigraphy of the Savannah logic Survey Information Circular 100, 26 p., 1 pi. in pocket. River Site and vicinity: Southeastern Geology, v. 35, no. 1, p. Litwin, R.J., Sohl, N.F., Owens, J.P., and Sugarman, P.J., 1993, 21-58. Palynological analysis of a newly recognized Upper Creta Frederiksen, N.O., 1979, Paleogene sporomorph biostratigraphy, ceous marine unit at Cheesequake, New Jersey: Palynology, v. northeastern Virginia: Palynology, v. 3, p. 129-167. 17, p. 123-135, pis. 1-3. ————1980, Paleogene sporomorphs from South Carolina and Mancini, E.A., Puckett, T.M., and Tew, B.H., 1996, Integrated bio- quantitative correlations with the Gulf Coast: Palynology, v. stratigraphic and sequence stratigraphic framework for Upper 4, p. 125-179. Cretaceous strata of the eastern Gulf Coastal Plain, USA: ————1988, Sporomorph biostratigraphy, floral changes, and Cretaceous Research, v. 17, no. 6, p. 645-669, 4 pis. paleoclimatology, Eocene and earliest Oligocene of the east Martini, Erlend, 1971, Standard Tertiary and Quaternary calcare ern Gulf Coast: U.S. Geological Survey Professional Paper ous nannoplankton zonation: Planktonic Conference, 2d, 1448, 68 p., 16 fossil pis., 2 pis. in pocket. Rome, 1969, Proceedings, p. 739-785. ————1991, Midwayan (Paleocene) pollen correlations in the Moshkovitz, Shimon, and Habib, Daniel, 1993, Calcareous nanno- eastern United States: Micropaleontology, v. 37, p. 101-123. fossil and dinoflagellate stratigraphy of the Cretaceous-Ter -1998, Upper Paleocene and lowermost Eocene angiosperm tiary boundary, Alabama and Georgia: Micropaleontology, v. pollen biostratigraphy of the eastern Gulf Coast and Virginia: 39, no. 2, p. 167-191, pis. 1-5. Micropaleontology, v. 44, p. 45-68. Gohn, G.S., 1992, Revised nomenclature, definitions, and correla Okada, Hisatake, and Bukry, David, 1980, Supplementary modifi tions for the Cretaceous formations in USGS-Clubhouse cation and introduction of code numbers to the low-latitude Crossroads #1, Dorchester County, South Carolina: U.S. Geo coccolith biostratigraphic zonation (Bukry, 1973; 1975): logical Survey Professional Paper 1518, 39 p., 1 pi. in pocket. Marine Micropaleontology, v. 5, no. 3, p. 321-325. Gradstein, P.M., Agterberg, PP., Ogg, J.G., Hardenbol, Jan, van Owens, J.P., Bybell, L.M., Paulachok, Gary, Ager, T.A., Gonzalez, Veen, Paul, Thierry, Jacques, and Huang, Zehui, 1995, A Tri- V.M., and Sugarman, P.J., 1988, Stratigraphy of the Tertiary assic, Jurassic and Cretaceous time scale, in Berggren, W.A., sediments in a 945-foot-deep corehole near Mays Landing in Kent, Dennis, Aubry, Marie-Pierre, and Hardenbol, Jan, eds., the southeastern New Jersey Coastal Plain: U.S. Geological Geochronology, time scales and global stratigraphic correla Survey Professional Paper 1484, 39 p. tion: SEPM (Society for Sedimentary Geology) Special Pub Owens, J.P, Minard, J.R, Sohl, N.F., and Mello, J.F., 1970, Stratig lication 54, p. 95-126. raphy of the outcropping post-Magothy Upper Cretaceous Greuter, W., Barrie, PR., Burdet, H.M., Chaloner, W.G., Demou- formations in southern New Jersey and northern Delmarva lin, V, Hawksworth, D.L., J0rgensen, P.M., Nicolson, D.H., Peninsula, Delaware and Maryland: U.S. Geological Survey Silva, PC., Trehane, P., and McNeill, J., 1994, International Professional Paper 674, 60 p. code of botanical nomenclature (Tokyo code): Regnum veget- Perch-Nielsen, Katharina, 1985, Mesozoic calcareous nannofos- abile, v. 131, 389+xviii p. sils, in Bolli, H.M., Saunders, J.B., and Perch-Nielsen, Katha Hazel, J.E., 1990, Major changes in Eocene and Oligocene Gulf rina, eds.. Plankton stratigraphy: New York, Cambridge Coast ostracod assemblages; relationship to global events, in University Press, p. 329^26. Whatley, Robin, and Maybury, Caroline, eds., Ostracoda and Pitakpaivan, Kasana, and Hazel, J.E., 1994, Ostracodes and chro- global events: London, Chapman and Hall, p. 113-121. nostratigraphic position of the Upper Cretaceous Arkadelphia Hazel, J.E., and Brouwers, E.M., 1982, Biostratigraphic and chro- Formation of Arkansas: Journal of Paleontology, v. 68, no. 1, nostratigraphic distribution of ostracodes in the Conia- p. 111-122. cian-Maastrichtian (Austinian-Navarroan) in the Atlantic and Prowell, D.C., Christopher, R.A., Edwards, L.E., Bybell, L.M., and Gulf Coastal Province, in Maddocks, R.F., ed., Texas Ostra Gill, H.E., 1985 [1986], Geologic section of the updip coastal coda, Guidebook of excursions and related papers for the plain from central Georgia to western South Carolina: U.S. Eighth International Symposium on Ostracoda: Houston, Geological Survey Miscellaneous Field Studies Map MF- University of Houston, p. 166-198. 1737, 10-p. text, 1 sheet. 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Ride, W.D.L., Sabosky, C.W., Bernard!, G., Melville, R.V., Corliss, Snipes, D.S., Fallaw, W.C., Price, Van, and Cumbest, R.J., 1993, J.O., Forest, J., Key, K.H.L. and Wright, C.W, 1985, Interna The Pen Branch fault; documentation of Late Cretaceous-Ter tional code of zoological nomenclature, third edition: Berke tiary faulting in the coastal plain of South Carolina: South ley, University of California Press, 321 p. eastern Geology, v. 33, no. 4, p. 195-218. Sohl, N.F., and Owens, J.P., 1991, Cretaceous stratigraphy of the Self-Trail, J.M., and Bybell, L.M., 1995, Cretaceous and Paleo- Carolina Coastal Plain, in Horton, J.W., Jr., and Zullo, V.A., gene calcareous nannofossil biostratigraphy of New Jersey, in eds., Geology of the Carolinas: Knoxville, Tenn., University Baker, J.E.B., ed., Contributions to the paleontology of New of Tennessee Press, p. 191-220. Jersey: Geological Association of New Jersey Contribution Summerour, J.H., Shapiro, E.A., Lineback, J.A., Huddlestun, P.P., Proceedings, v. 12, p. 102-139. and Hughes, A.C., 1994, An investigation of tritium in the Self-Trail, J.M., and Gohn, G.S., 1996, Biostratigraphic data for Gordon and other aquifers in Burke County, Georgia: Georgia the Cretaceous marine sediments in the USGS-St. George No. Geologic Survey Information Circular 95, 93 p. 1 core (DOR-211), Dorchester County, South Carolina: U.S. Van Nieuwenhuise, D.S., and Colquhoun, D.J., 1982, The Pale- Geological Survey Open-File Report 96-684, 29 p. ocene-lower Eocene Black Mingo Group of the east-central Siple, G.E., 1967, Geology and ground water of the Savannah coastal plain of South Carolina: South Carolina Geology, v. River Plant and vicinity, South Carolina: U.S. Geological Sur 26, no. 2, p. 47-67. Wolfe, J.A., 1976, Stratigraphic distribution of some pollen types vey Water-Supply Paper 1841, 113 p. from the Campanian and lower Maestrichtian rocks (Upper Sissingh, W., 1977, Biostratigraphy of Cretaceous calcareous nan- Cretaceous) of the Middle Atlantic States: U.S. Geological noplankton: Geologic en Mijnbouw, v. 56, p. 37-65. Survey Professional Paper 977, 18 p., 4 pis.

U.S. Department of the Interior U.S. Geological Survey

Palynomorph Biostratigraphy and Paleoecology of Upper Cretaceous Sediments from Four Cores from Screven and Burke Counties, Georgia By Norman 0. Frederiksen, Lucy E. Edwards, and Ronald J. Litwin

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract...... Cl Introduction...... 1 Acknowledgments...... 2 Material and Methods ...... 2 Lithostratigraphy and Previous Biostratigraphy...... 2 Millhaven Test Hole...... 10 Cape Fear Formation...... 10 Middendorf Formation...... 10 Subunit2...... 10 Black Creek Group ...... 10 Subunitl...... 10 Subunit2...... 14 SubunitS...... 16 Steel Creek Formation ...... 16 Girard Test Hole...... 20 Cape Fear Formation...... 20 Middendorf Formation...... 20 Subunitl...... 20 Subunit2...... 20 Black Creek Group ...... 23 Steel Creek Formation ...... 23 Thompson Oak Test Hole ...... 23 Black Creek Group ...... 24 Millers Pond Test Hole ...... 24 Cape Fear Formation...... 24 Middendorf Formation...... 26 Black Creek Group ...... 26 Summary...... 29 References Cited...... 30

PLATES [Plates follow References Cited]

1-5. Pollen. 6. Dinoflagellates and acritarchs. 7. Dinoflagellates.

FIGURES

1. Index map showing the S avannah River Site and locations of stratigraphic test holes in the study area...... C2 2. Chart showing European stage assignments of Coniacian to Maastrichtian formations in New Jersey and the main pollen zonations proposed for these formations ...... 6 3. Chart showing pollen taxa occurrences in 11 samples between 1,212.0 and 733.2 ft in the Millhaven core, Screven County, Ga...... 11

III IV CONTENTS

4. Chart showing dinoflagellate taxa occurrences in 10 samples between 1,212.0 and 680.8 ft in the Millhaven core, Screven County, Ga...... 12 5-10. Chart showing known stratigraphic ranges of pollen taxa in the Millhaven core, Screven County, Ga.: 5. Sample R4664 CA, subunit 1 of the Black Creek Group, from 1,124.3-1,124.7 ft...... 13 6. Sample R4664 BB, subunit 2 of the Black Creek Group, from 1,029.5 ft...... 14 7. Sample R4664 FD, subunit 2 of the Black Creek Group, from 941.7-941.9 ft...... 15 8. Three samples (R4664 CD, DA, and FE) from the Steel Creek Formation between 830.5 and 824.1 ft...... 17 9. Sample R4664 GA, Steel Creek Formation, from 769.0-769.3 ft...... 18 10. Sample R4664 CF, Steel Creek Formation, from 733.2-733.3 ft...... 19 11. Chart showing pollen taxa occurrences in three samples between 1,139.0 and 738.3 ft in the Girard core, Burke County, Ga...... 20 12. Chart showing dinoflagellate taxa occurrences in 15 samples between 1,139.0 and 720.3 ft in the Girard core, Burke County, Ga...... 21 13-15. Charts showing known stratigraphic ranges of pollen taxa in the Girard core, Burke County, Ga.: 13. Sample R4705 AA, subunit 1 of the Middendorf Formation, from 1,138.0-1,139.0 ft...... 22 14. Sample R4705 BA, subunit 2 of the Middendorf Formation, from 1,012.0-1,012.3 ft...... 22 15. Sample R4705 BG, subunit 2 of the Black Creek Group, from 738.3-738.6 ft...... 23 16. Chart showing dinoflagellate taxa occurrences in two samples from 561.0 and 505.0 ft, respectively (Black Creek Group), in the Thompson Oak core, Burke County, Ga...... 24 17. Chart showing pollen taxa occurrences in four samples between 832.0 and 517.0 ft in the Millers Pond core, Burke County, Ga...... 25 18-20. Charts showing known stratigraphic ranges of pollen taxa in the Millers Pond core, Burke County, Ga.: 18. Sample R4581 B, Cape Fear Formation, from 827.0-832.0 ft...... 26 19. Sample R4581 C, Cape Fear Formation, from 797.0-802.0 ft...... 27 20. Sample R4581 I, Black Creek Group, from 517.0 ft...... 28

TABLES

1. Pollen and dinoflagellate occurrences in samples from the Upper Cretaceous units of the Millhaven, Girard, Thompson Oak, and Millers Pond cores, Screven and Burke Counties, Georgia...... C3 2. Coordinates of photographed pollen specimens on Leitz microscope 871956 at the U.S. Geological Survey, Reston, Virginia...... 4 3. Coordinates of photographed dinoflagellate and acritarch specimens on Olympus Vanox microscope 201526 at the U.S. Geological Survey, Reston, Virginia...... 5 4. List of pollen taxa mentioned in this paper with some synonyms ...... 7 5. List of dinoflagellate and acritarch taxa mentioned in this paper ...... 9 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Palynomorph Biostratigraphy and Paleoecology of Upper Cretaceous Sediments from Four Cores from Screven and Burke Counties, Georgia

By Norman O. Frederiksen, Lucy E. Edwards, and Ronald J. Litwin

ABSTRACT core appear to be Maastrichtian in age. One sample from the Steel Creek Formation may have at least marginal-marine Fifty-two Upper Cretaceous samples were examined dinoflagellates. All Cretaceous samples from the most for palynomorphs (pollen grains and dinoflagellates) from updip Millers Pond core lack dinoflagellates. four cores (Millhaven, Girard, Thompson Oak, and Millers Pond) from Screven and Burke Counties, Georgia. Two pol len-bearing samples from the Cape Fear Formation of the INTRODUCTION Millers Pond core are both of Coniacian or early Santonian age. At the Savannah River Site (SRS) in Aiken, Barnwell, Three pollen-bearing samples were obtained from the and Allendale Counties, S.C. (fig. 1), various hazardous overlying Middendorf Formation of the Millhaven and materials have been manufactured, disposed of, and stored Girard cores; one of them is Coniacian or Santonian, one since the early 1950's. The U.S. Geological Survey, in coop apparently is latest Santonian(?) or earliest Campanian, and eration with the U.S. Department of Energy and the Georgia one sample is of uncertain age. Dinoflagellate data indicate Geologic Survey of the Georgia Department of Natural that the Middendorf Formation in the Millhaven core repre Resources, is conducting a study of the subsurface geology, sents, at least in part, marginal or very near shore marine hydrology, and water quality in the vicinity of the SRS with conditions, whereas the Middendorf of the updip Girard the goal of understanding the present and possible future core appears to be entirely nonmarine. ground-water flow in the aquifers of the area. Seven samples from the Black Creek Group (overlying Many test holes have been drilled in Georgia and the Middendorf Formation) of the Millhaven, Girard, and South Carolina to study the flow of ground water in the SRS Millers Pond cores had usable pollen assemblages, and region (Aadland, 1992; Harris and others, 1992; Strom and these are mid-Campanian to possibly Maastrichtian. Marine others, 1992; Clarke, 1993; Gellici andLogan, 1993; Clarke strata, particularly in the middle part of the Black Creek and others, 1994, 1996; Clarke and West, 1994; Leeth and Group in the Millhaven, Girard, and Thompson Oak cores, others, 1996). The Cretaceous and Cenozoic aquifers are contain late Campanian dinoflagellates. The Black Creek difficult to correlate from area to area because of structural Group in the Millhaven core represents (in upward movement and rapid facies changes. Some biostratigraphic sequence) marginal or very near shore marine conditions research has been completed toward the goal of correlating (subunit 1) and normal marine to nearshore marine condi aquifers between some of the test holes (for example, Prow- tions (subunits 2 and 3). The Black Creek in the more updip ell, Edwards, and Frederiksen, 1985; Edwards, 1992; Girard core represents nonmarine, then nearshore marine, Edwards and Clarke, 1992; Edwards and Frederiksen, 1992; then nonmarine deposition. Two samples from the Black Lucas-Clark, 1992; Falls and others, 1993,1997; Clarke and Creek Group in the still more updip Thompson Oak core others, 1994, 1996; Leeth and others, 1996; Edwards and represent, in ascending order, apparent nonmarine and near- others, 1997), but much biostratigraphic study remains to be shore marine paleoenvironments, respectively. done in the region. Five pollen-bearing samples from the Steel Creek For Palynomorphs are abundant and well-preserved fossils mation (overlying the Black Creek Group) of the Millhaven in some of the Cretaceous subsurface sediments in the SRS

Cl C2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA 8230 82 8130 MATERIAL AND METHODS

The core samples discussed in this paper were cleaned and scraped and then treated in hydrochloric acid and hydrofluoric acid to remove carbonate and silicate material, respectively. Samples were then oxidized in nitric acid and 33° 30' centrifuged in laboratory detergent to remove fine debris. •:":• y ':. ' yX Sample residues were stained in Bismark brown and ,' .'/' 'Barnwe Savannah ' screened on 8- or 10-micrometer ((am) sieves for pollen and :.'••. River •'X Site :'• on 20-|om sieves for dinoflagellates. The residues were swirled in a watch glass and mounted on slides in glycerin jelly for light-microscope observation. 33° In table 2, which shows the slide numbers and micro scope coordinates of photographed pollen specimens, the slide designations show the sample number with the slide number in parentheses. Coordinates locate the specimens on Leitz microscope 871956 at the U.S. Geological Survey, Reston, Va. On this microscope, the coordinates for the cen 32°30'- ter point of a standard 25.4x76.2-millimeter (mm) slide are 38.8 and 102.5 for the horizontal and vertical axes. The hor izontal coordinates increase toward the right edge of the

Millhaven stage, and the vertical coordinates increase toward the front • Test hole site and informal name of site of the stage. The slide numbers and microscope coordinates of pho tographed dinoflagellates (table 3) locate the specimens on Figure 1. Index map showing the Savannah River Site and Olympus Vanox microscope 201526 at the U.S. Geological locations of stratigraphic test holes in the study area. Survey, Reston, Va. On this microscope, the coordinates for the center point of a standard 25.4x76.2-mm slide are 27.5 region. Palynomorphs include pollen grains and spores from and 112.7 for the vertical and horizontal axes. The vertical terrestrial plants as well as the cysts—or in a few cases, per coordinates increase as the stage is moved up, and the hori haps thecae—of mainly marine dinoflagellates. The purpose zontal coordinates increase as the slide is moved from left to of this paper is to use Cretaceous palynomorphs in core right. samples to provide biostratigraphic and paleoenvironmental All palynological slides are stored at the U.S. Geologi data on both marine and nonmarine sediments in the area. cal Survey, Reston, Va. The core samples were taken from four Georgia test holes (Millhaven, Girard, Thompson Oak, Millers Pond) in Screven and Burke Counties, Ga., directly across the Savan LITHOSTRATIGRAPHY AND nah River from the SRS. Table 1 summarizes the number of PREVIOUS BIOSTRATIGRAPHY samples examined from each stratigraphic unit in each test hole. Details of the geologic framework are presented else where (Falls and Prowell, this volume, chap. A). Falls and Prowell recognize three formations and one group within ACKNOWLEDGMENTS the Cretaceous, and their terminology and correlations are followed here. The Cape Fear Formation is the lowermost unit studied and consists of partially lithified to unlithified, We thank U.S. Geological Survey colleagues John S. poorly to very poorly sorted clayey sand and sandy clay. It is Clarke, W. Fred Falls, R. Parley Fleming, Gregory S. Gohn, overlain by the Middendorf Formation, a poorly consoli and David C. Prowell, as well as Paul F. Huddlestun (Geor dated, poorly sorted sand that contains thin clay beds; Falls gia Geologic Survey, Atlanta) and palynological consultant and Prowell (this volume, chap. A) divide the Middendorf Joyce Lucas-Clark (Fremont, Calif.) for the sharing of data into two informal subunits. Above the Middendorf Forma and ideas and the sometimes lively discussions that helped tion, Falls and Prowell (this volume, chap. A) recognize the shape the ideas in this paper. We are grateful to Raymond A. Black Creek Group, which they divide into three informal Christopher (Clemson University) and G.S. Gohn for very subunits that do not coincide with named formations that helpful reviews of the first draft of this paper. have been studied elsewhere. The uppermost Cretaceous PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C3 Table 1. Pollen and dinoflagellate occurrences in samples from the Upper Cretaceous units of the Millhaven, Girard, Thompson Oak, and Millers Pond cores, Screven and Burke Counties, Georgia. [Sample depths are in feet below land surface. Symbols in the last four columns are defined next. P (pollen) column: Y (yes), sample contains pollen that is biostratigraphically useful; N (no), sample contains pollen that is not biostratigraphically useful; C, sample contains contaminants only; o, pollen was observed in the sample but not studied. D (dinoflagellate) column: Y (yes), has dinoflagellates; C, has only contaminant dinoflagellates; o, dinoflagellates were observed in the sample but not studied. B (barren) column: X, sample is barren of all palynomorphs. ND (no dinoflagellates) column: X, sample was examined for dinoflagellates, but none were found; however, at least some pol len was observed in the sample]

Sample Depth R number (ft) Unit (subunit) P D B ND Millhaven core, Screven County, Ga. R4664CG— — — — 680.8-681 Steel Creek x R4664 CF 733.2-733.3 Steel Creek Y X 755-755.3 Steel Creek C Y?C R4664GB— ----- — - 755.3 755.6 Steel Creek C C R4664 CE 768.8-769 Steel Creek X — R4664 GA 769.0-769.3 Steel Creek Y R4664 FF 789.7-790 Steel Creek x R4664 FE— — — — - 824.1-824.4 Steel Creek Y X DA.&&A F>A QOQ <: Q9Q Q Steel Creek Y R4664 CD OQA Q QQA. ^ Steel Creek Y Y R4664 CC 849.3-849.6 Black Creek Group (3) N Y — R4664 CB 913.8-914.2 Black Creek Group (3) Y Y 941.7-941.9 Black Creek Group (2) Y Y R4664 BB 1029.5 Black Creek Group (2) Y Y R4664CA— — — — Black Creek Group (1) Y Y — R4664BA— ----- — - 1212 Middendorf(2) Y Y Girard core, Burke County, Ga.

TJ/J TAC rjTJ 720.3-720.5 Black Creek Group (3) 0 X R4705BG— — — — Black Creek Group (2) Y Y R4705 CE — — — — 784-784.3 Black Creek Group (2) o Y R4705 CD— ------— 799.7-799.9 Black Creek Group (2) 0 0 R4.70.S CC 822.8-823 Black Creek Group (2) R4705 CB 834.6-834.8 Black Creek Group (2) o Y R4705CA— — — — 859.5-859.8 Black Creek Group (2) R4705 BF — — — — Black Creek Group (2) o Y D /nnc rjn? 883.5-883.8 Black Creek Group (2) o X R4705 DD— — — — 910-910.5 Black Creek Group (1) o X R4705 BD— — — — 924.8-925.2 Black Creek Group (1) o X R4705BC— — — — ca. 960? Middendorf(2) y R4705 DC 993.5-994 Middendorf (2) x R4705BA— — — — 1012 1012.3 Middendorf (2) Y X R4705DB— — — — 1013 Middendorf (2) o X R4705AC— ----- — - Middendorf (2) o X R4705DA— — — — 1046.6-1047 Middendorf (2) o X R4705AB— — — — 1063 Middendorf (1) x R4705 AA— — ------1138-1139 Middendorf (1) Y X Thompson Oak core, Burke County, Ga. D A QO f. T3 505 Black Creek Group o Y — R4836A— - — — — 561 Black Creek Group o Y Millers Pond core, Burke County, Ga. R4581 O TOO TQ7 Steel Creek X R4581 N— — — ----- 332-337 Black Creek Group x R4581 M — — — — - 397-402 Black Creek Group x P/1CC1 T 447-453 Black Creek Group x P/1CC1 17- 481 Black Creek Group x P/1CC1 T 497.5 Black Creek Group y — R4581I— — — — — 517 Black Creek Group Y n A Co i TJ 557.5-558 Black Creek Group N R4581 G— — — ----- 578 Black Creek Group Y P/1CS1 T7 608 Middendorf X — n A CO 1 "R 662-671 Middendorf x R4581 D 778 Cape Fear x R4581 C 7Q7 cm Cape Fear Y — D A co i rj 827-832 Cape Fear Y T?4S21 A 847-852 Cape Fear x — C4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Table 2. Coordinates of photographed pollen specimens on Leitz microscope 871956 at the U.S. Geological Survey, Reston, Virginia.

Figure Sample R no. (slide no.) Coordinates Figure Sample R no. (slide no.) Coordinates Plate 1 Plate 3 1 ..„__._._.„.__.. R4.70^ A AfS^ uvj.u60 6 YA. Q4.y-r.y Q 1 ...... -__.__— R4705 AA(5) 58.0x96.8 9 R4664 DA(3) 56.3 x 103.0 2———————— R4664 CA(6) 53.7 X 102.5 a R4664FE(1) 55.5x103.0 0 R4664 CA(6) 60 4. v Q4 7 4 ._.„_...._„___.. R4581 1(5) 55.2 x 108.0 4, 5——..————— R4664 CA(6) 66.4x101.6 5 —— ——— —— R4664FE(1) 50.1 x 105.2 6 ^7 p/ICQI (~<(1\ 51.8x102.6 6, 7 —-———. R4664 DA(3) ao i v 1f)Q Q p/ICQI p/1 \ 54.6 x 102.3 R4664 CD(4) 65.3 x 100.3 Q R4581 1(5) 61 4 v 101 Q R4664 DA(3) 56.5x112.1 10,11—————— R4581 1(5) ^R f) v QQ 9 10————— R4664FE(1) 58.6x110.3 12——————— R4664 GA(1) 56.2x111.0 11——————— R4664 DA(3) 54.0x107.8 13——————— R4664 GA(1) 54.0x101.2 12 __ ___ . R4664FE(1) 60.6 x 95.7 14 15- - ___ — R4705 BG(4) 62.1x94.8 1 ^ R4705 BG(4) 50 2 x 99 4 16—————— R4664 GA(1) 51.8x108.4 14 ._...... „..... R4664FD(1) 59.5 x 96.4 P lilt A d 15, 16 —— — — R4664 DA(3) 54.8x101.7 1 2 ____ - _ - R4664 DA(3) 33.3x101.2 R4664GA(1) 55.1x102.1 3—— ...... — —— R4581 1(5) 59.6 x 106.6 1 8 R4664 CA(6) 54.8x99.8 4——— ...... ______R4705 BA(4) 58.3x94.6 19 21 _ — — R4664GA(1) 62.3x105.1 5—— ______R4705 BA(4) 60.6 x 100.9

A Id 1C £t 6—— — —— — — R4581 C(l) 56.7x103.0 1 — ______.„__._. R4664FD(1) 49.9x110.3 7———————— R4664 GA(1) 53.0x93.8 2 ...... — — . R4664 DA(3) CO 7 v QC 0 R4705 AA(5) 61.9 x 107.6 3, 4 ——— ——— . R4664FD(1) 52.2 x 105.8 9———— .... R4705 BA(4) 60.0 x 102.4 <; R4581 1(5) 56.5x111.5 10, 11————— R4705 BA(4) 39 9 v 11 1 6 6 ^7 R4664GA(1) «7 o v QQ O 12 13- - ___ — R4705 AA(5) 49.6 x 97.3 T?/tS81 f~Y1 \ S.f. « v Q^ 9 14 15—————— R4664 DA(3) 0/1 0 v 1 AC 0 Q TJ/ICQ 1 /~V1 \ 60.5 x 95.3 Plofp C 10—————— D/l co 1 T3/"1 \ 45 9 x 97 3 1— __...... — R4705 BG(4) 52.4x103.1 11...... R4705 BA(4) 50.2 x 106.2 R4664 BB(5) S4. 8 v QR 3 12 ______. p/ico i /"'('i \ ^7 D v Q4. 9 3— ______— — R4664 BB(5) 57 5 X 1 1 1 4 1 ^ p/icoi pvi"> 5.4. 6 Y QQ 1 4, 5— ...... R4705 BG(4) 61.2x110.5 14———————. R 4.664. C &(f\\ 64.1 X 104.4 6, 7— ——— ------R4705 AA(5) 60.5 x 97.8 15——————. D/l ^O 1 Ttfl \ «o « v Q^ 9 8, 9— — — — — — - R4664FE(1) eg c v no 7 16—————. R4664FD(1) S 1 9 v 1 f)7 4. 10, 11—————— R4664 CD(4) 50.3 x 107.7 17 19 ———— TJ/I CO 1 TJ/-1 \ S6 ^ v Q7 3 12 13 ____ - - R4664 CD(4) S5 7 v 1 19 1 20 _ ____ R4664 CA(6) 42.8x93.3 14 ______R4705 BA(4) ^8 7 v QQ Si 21 __ __ ... D/lcoi (~*f]\ 58.5 x 102.6 unit, where present, is the Steel Creek Formation, a poorly Of particular importance to our work is the placement sorted sand and clay. of the Campanian-Maastrichtian boundary at the first appearance datum of the ammonite Pachydiscus neuber- In this paper, age determinations for samples from the gicus (von Hauer) in the Teras Quarry, France. This bound Upper Cretaceous of Georgia are made using pollen and ary position is stratigraphically higher (younger) than some dinoflagellate taxa. The chronostratigraphic ranges of these previous interpretations of the boundary. When this bound fossils are known on the basis of previous work mainly in ary is correlated using nannofossil and foraminiferal zones, the Middle Atlantic States. European stage assignments and some strata that were previously considered to be Maas- ages of Upper Cretaceous formations in New Jersey (fig. 2) trichtian should now be considered to be upper Campanian. are based primarily on calcareous nannofossil correlations, For example, the Mount Laurel Formation of New Jersey but the relation between calcareous nannofossil zones and was considered by some earlier authors (for example, Ols- European stages is subject to revision. Here, we use the son and others, 1988; Aurisano, 1989) to be lower Maas- boundary proposals summarized by Burnett (1996) from the trichtian. However, the Mount Laurel Formation has been Second Symposium on Cretaceous Stage Boundaries, Brus assigned to calcareous nannofossil Zone CC 22 (Self-Trail sels, 1995. and Bybell, 1995; Sugarman and others, 1995), and Burnett PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C5

Table 3. Coordinates of photographed dinofla; jellate and acritarch specimens on Olympus Vanox microscope 201526 at the U.S. Geological Survey, Reston, Virginia. Figure Sample R no. (slide no.) Coordinates Figure Sample R no. (slide no.) Coordinates Plate 6 Plate 7 — Continued 1 ______R4705 BG(3) 32.8 X 100.0 3 ..„.„.„.....„ R4664 BA(4) 26.7 x 84.3 2 ______R4664 BB(4) 30.1x97.8 4 ______R4664 BA(4) 70 7 v Q4 ? 3 ______R4705 BF(3) 35.5 x 86.9 5 —————— R4664 BB(4) 23.3x99.6 4—— ______R4664 BB(4) 26.4x96.1 6 ... ——— ——— R4705 CB(4) 11 i \/ en o 5 ______R4664 CB(3) 37.0x83.5 7 __„______„_„ R4664 CD(3) 22.3 x 106.7 6——————— R4705 BF(2) 32.5 x 99.2 8, 9 -————- R4705 CB(4) 30.2 x 89.0 7 ______R4705 BG(3) 29.2 x 72.0 10—————— R4664 CA(4) 36.8x76.4 R4664 BB(4) 24.2 x 99.7 11——————— R4664 BB(4) 36.0x108.0 9 ______R4664 BB(4) 24.4 x 77.5 12—————— R4705 BF(2) 26.1x72.0 10—————— R4664 CB(4) 20.3 x 105.2 13..-...... —. R4705 BG(3) 30.1x72.1 11— ______R4705 BG(3) 37.1x101.5 14— ______R4705 BG(3) 36.0x103.7 1 2 ______R4705 BF(2) 25.6 x 90.8 15— ______R4664 CA(4) 35.8 x 102.0 13-—————— R4705 BF(2) 34.4x69.6 16—————— R4664 CA(4) 32.3x73.7 14———— ...... R4664 CB(3) 34.8 x 95.9 17——————— R4664CB(3) 32.7 x 100.5 15—— —— ______R4705 BF(2) 20.0 x 105.3 18—————— R4664 BB(4) 28.7x95.9 16—————— R4705 BG(3) 31.7x108.9 19— ______R4836 B(3) 30.3x77.4 Plate 7 20—————— R4664 BB(4) 28.7x97.8 1 ______„______. D/nn? Taij/"")\ 32.5 x 84.4 21—————— R4705 CB(4) 32.2x81.4 9 ______RA£fiARA<7h 11 1 v 7^ fi

(1996) placed the Campanian-Maastrichtian boundary Atlantic States. The base of pollen Zone V (fig. 2) occurs in within the lower part of Zone CC 23; therefore, we agree the lowermost part of the Austin Chalk of Texas (Christo with Self-Trail and Bybell (1995) and Sugarman and others pher, 1982c), which is Coniacian (Sohl and others, 1991). (1995) in assigning the Mount Laurel Formation to the The top of Zone V is Santonian (Christopher and others, upper Campanian (fig. 2). 1997). The South Amboy Fire Clay Member, which forms Sugarman and others (1995) provided nannofossil the upper part of the Raritan Formation in New Jersey, has zonal assignments for the Navesink Formation and for the not been dated by means of marine fossils; therefore, the lower part of the Red Bank Sand of New Jersey. Self-Trail age determinations of Christopher (1977a), as modified by and Bybell (1995) gave nannofossil zonal assignments for Christopher (1982c), are used for this member. Aurisano's the Merchantville, Englishtown, Marshalltown, Mount Lau (1989) suggestion that the South Amboy Fire Clay Member rel, and Navesink Formations. Self-Trail and Bybell pre should be reassigned from the Raritan to the Magothy For sented these stage assignments in terms of Perch-Nielsen's mation appears to be a good idea, but for purposes of the (1985) calcareous nannofossil zonation, but Self-Trail (writ present paper, the South Amboy Fire Clay Member is ten commun., 1996) has translated her zonal assignments retained in the Raritan Formation. into the zonal and stage scheme of Burnett (1996), which is followed here. In this paper, age determinations are based on pollen European stage assignments of Upper Cretaceous for range charts presented by Tschudy (1973, 1975), Wolfe mations in the Gulf Coast were summarized by Sohl and (1976), Christopher (1978, 1979), Frederiksen and Christo others (1991) on the basis mainly of mollusk, planktonic pher (1978), and Litwin and others (1993), with some foraminiferal, and calcareous nannofossil data. Tschudy occurrence and range data from additional publications (for (1973, 1975) and Christopher (1982b,c) instead used pollen example, Tschudy, 1970; Christopher and others, 1979; taxa to correlate these Gulf Coast stratigraphic units with Christopher, 1980). We have preferred to use the better those of the Atlantic Coastal Plain and of Europe. known Atlantic Coastal Plain stratigraphic ranges rather The standard pollen zonation for the Upper Cretaceous than Gulf Coast ranges. However, it appears that some pol of the Gulf and Atlantic Coastal Plains (fig. 2) has been len taxa have somewhat different stratigraphic ranges in the developed in a series of abstracts and papers, notably those Carolinas and Georgia than they have in the Middle Atlantic of Doyle (1969), Sirkin (1974), Wolfe (1976), Doyle and States. This regional difference may account for difficulties Robbins (1977), and Christopher (1977b, 1982c). This in making age determinations for some samples in this zonation was based on material mainly from the Middle paper (R.A. Christopher, written commun., 1996). Similar C6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

POLLEN POLLEN POLLEN ZONATION ZONATION OF ASSEMBLAGE-ZONES OF WOLFE CHRISTOPHER OF CHRISTOPHER (1976) (1977b) (1979) SUB- SUB- ZONE ZONE ZONE ZONE

MT. LAUREL FM. WENONAH FM.

NO DATA NO DATA CA-5

MARSHALLTOWN FM.

ENGLISHTOWN FM. CA-4

WOODBURY CLAY CA-3

MERCHANTVILLE FM. CA-2

UNNAMED MARINE BEDS NO DATA "CA^T "CLIFFWOOD BEDS" tPSEUDOPLICAPOLLIS CUNEATA- "MORGAN BEDS" SEMIOCULOPOLLIS VERRUCOSA MAGOTHY FM . AMBOY STONEWARE CLAY MBR PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA OLD BRIDGE SAND MBR. COMPLEXIOPOLLIS EXIGUA- RARITAN FM. SOUTH AMBOY FIRE CLAY MBR. SANTALAC1TES MINOR (PART)

Figure 2. Chart showing European stage assignments of shown is the tentative assignment of the unnamed marine Coniacian to Maastrichtian formations in New Jersey and beds to Zone CA-2A by Litwin and others (1993). FM., the main pollen zonations proposed for these formations. Formation, MBR., Member. Sources of the stage assignments are given in the text. Not differences in marine coccolith floras between New Jersey from South Carolina from the same stratigraphic units that and Georgia are reported by Bukry (this volume, chap. D). are present in the Georgia cores discussed here. The study Most of the pollen taxa mentioned in this report (table by Firth (1987) in western Georgia dealt with dinoflagel 4) have been illustrated previously in the publications listed, lates near the Cretaceous-Tertiary boundary. but many of the taxa are also illustrated in this report (plates Dinoflagellates from the Atlantic Coastal Plain have 1-5). been described by several authors, including Koch and Ols- Relatively little has been published on the dinoflagel- son (1977), Whitney (1979), May (1980), and Aurisano lates from Upper Cretaceous sediments of the Eastern (1989). The dinoflagellate succession described by May United States. Early work in Texas (Zaitzeff and Cross, (1980) from the Mount Laurel Formation in the Atlantic 1971) has been supplemented by recent papers by Srivastava Highlands in New Jersey is of particular relevance. Some of (1991, 1993) and Cretaceous-Tertiary boundary studies by the key dinoflagellate taxa from the present samples are Habib and others (1996). Papers by Habib and Miller (1989) illustrated in plates 6 and 7, and the dinoflagellate and acri- and Lucas-Clark (1992) list some of the dinoflagellates tarch taxa mentioned in this report are listed in table 5. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C7

Table 4. List of pollen taxa mentioned in this paper with some synonyms.

Taxon Plate Figure Brevicolporites sp. ——————————————————————————————————————— 3 14, 15 Brevicolporites sp. A of Christopher (1978); see CP3F-1 ———————————————— — — Casuarinidites sp. A of Frederiksen and Christopher (1978) = Triatriopollenites ruren- sis Pflug & Thomson in Thomson and Pflug (1953) of Gray and Groot (1966) —— 1 14, 17 Casuarinidites sp. ——————————————————————————————————————— — — Complexiopollis abditus Tschudy = NB-1 of Wolfe (1976)——————————— 2 11 Complexiopollis exigua Christopher————————————————————————————— — — Complexiopollis funiculus Tschudy ————————————————————————————— 2 10 Complexiopollis sp. D of Christopher (1979) ——————————————————————— — — Complexiopollis sp. E of Christopher (1979)—————————————————————— — — Complexiopollis sp. H of Christopher (1979) —————————————————————— — — Complexiopollis sp. I of Christopher (1979) ———————————————————————— — — Complexiopollis sp. ———————————————————————————————————— 2 12 Complexiopollisl sp.—————————————————————————————————————— 2 17-19 C3A-2 of Wolfe (1976) ————————————————————————— — — Aff. C3C-1 of Wolfe (1976)——————————————————————— 4 7 CP3B-1 of Wolfe (1976)——————————————————————————— — — CP3B-6 of Wolfe (1976) ————————————————————————————— — — CP3D-1 of Wolfe (1976)—————————————————————————— — — CP3D-3 of Wolfe (1976) = Holkopollenites cf. H. chemardensis Fairchild in Stover and others (1966) of Christopher (1978)———————————————————— 4 3 5 1-3 CP3E-1 of Wolfe (1976) = 1 Holkopollenites sp. of Christopher (1978) —————— 4 12, 13 5 4-9 CP3F-1 of Wolfe (1976) in part = Brevicolporites sp. A of Christopher (1978) ——— 3 12, 13 4 1,2 4 4,5 CP3F-2 of Wolfe (1976) = Brevicolporites sp. B of Christopher (1978)—————— — — CP3G-1 of Wolfe (1976)—————————————————————————— 4 8 Holkopollenites spp. —————————————————————————————————————— 4 14, 15 5 14 Interporopollenites turgidus Tschudy ———————————————————————————— 2 2 Labrapollis sp. B of Christopher (1979) ———————————_.__.__.__.——.__.__. — — Lanagiopollis cribellatus (Srivastava) Frederiksen = CP3A-3 of Wolfe (1976) = Tri- colporites sp. C of Christopher (1980)——————————————————— 3 16 Libopollis sp.—————————————————————————————————————————— — — Momipites fragilis Frederiksen & Christopher——————————————————————— — — Momipites microfoveolatus (Stanley) Nichols = NK-3 of Wolfe (1976) ———————— 1 3 Momipites tenuipolus group of Frederiksen and Christopher (1978) = NK-2 of Wolfe (1976)------———————————— 1 5 Momipites sp. H of Christopher (1979) ——————————————————————————— — — Momipites sp. I of Christopher (1979) —————————————————————————— — — Momipites n. sp. 1 ————————————————————————————————————— 1 6, 7 1 10-12 Cf. MPH-1 of Wolfe (1976) ———————————————————————— 5 10, 11 New genus A of Tschudy (1975)————————————————————-— 2 13 New genus D, sp. B of Christopher (1979) —————————————————— 2 21 C8 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Table 4. List of pollen taxa mentioned in this paper with some synonyms—Continued.

Taxon Plate Figure New genus D, sp. H of Christopher (1979) —————————————————— 2 20 New genus D, sp. J of Christopher (1979)——————————-———————— 3 i New genus D, sp. L of Christopher (1979) ————————————————— 3 2 N20-2 of R. A. Christopher (unpublished) —————————————————— 3 3-5 N20-12of R.A. Christopher (unpublished)————————————————------1 13 NB-2 of Wolfe (1976) = Complexiopollis sp. of Christopher (1978) ——————— — — NB-3 of Wolfe (1976)——————————————————————————— — — Cf. ND-2 of Wolfe (1976) ———————————————————————— 2 16 NF-1 of Wolfe (1976) = Trudopollis sp. A of Christopher (1978) ————————— — — NO-3 of Wolfe (1976) = Betulaceoipollenites sp. of Christopher (1978) —-———— — — NP-1 of Wolfe (1976) = Triatriopollenites sp. A of Christopher (1980)—————— — — NP-2 of Wolfe (1976) = Triatriopollenites sp. of Christopher (1978) = Triatriopolleni tes sp. B of Christopher (1980) ~~—-~—~_~_~__-~~~~—------1 8, 9 Nyssapollenites sp. of Christopher (1982b) ——————————————————————— — — Nyssapollenites sp.——————————————————————————————————————— 4 10, 11 Plicapollis sp. A of Christopher (1979)————-—————————————— 2 8 Plicapollis sp. K of Christopher (1979)—————-————————————— 2 9 Plicatopollis cretacea Frederiksen & Christopher = NN-2 of Wolfe (1976) ————— — — IPorocolpopollenites sp. A of Christopher and others (1979) ————————————— 3 6, 7 Porocolpopollenites n. sp. 1 ————————————————————————————————— 3 8 Praecursipollis plebius Tschudy——————————————————————————————— 2 14, 15 Proteacidites sp. aff. PR-3 of Wolfe (1976) ————————————————— — — PR-1 of Wolfe (1976) = Proteacidites sp. B of Christopher (1978) ——————— 1 18 2 1 PR-5 of Wolfe (1976) = Proteacidites sp. C of Christopher (1978) ——————— — — PR-7 of Wolfe (1976) = Proteacidites sp. A of Christopher (1978) = Proteacidites sp. G of Christopher (1980) ————————————————————————— 1 15, 16 Rhombipollis sp.———————————————————————————————————————— 3 10, 11 Rugubivesiculites sp. ————————————————————————————————————— 1 1 Santalacites minor Christopher ————————————————————————————— — — Tetracolporate sp. ——————————————————————————— 5 12, 13 Triatriopollenites spp. ————————————————————————————————————— 1 2, 4 Tricolpites spp. ———————————————————————————————————————— 2 5-7 Tricolporites sp. ———————————————————————————————————————— 4 6, 9 Cf. Triporate type 4 of Christopher (1979) ——————————————————— 1 19-21 Trisectoris costatus Tschudy ————————————————————————————————— 2 3,4 Trudopollis sp. cf. T. meekeri Newman ——————————————————————————— 3 9 PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C9

Table 5. List of dinoflagellate and acritarch taxa mentioned in this paper.

Taxon Plate Figure Alisogymnium-Dinogymnium spp. = specimens representing various species of the genera Alisogymnium Lentin & Vozzhennikova 1990 and Dinogymnium Evitt et al. 1967 —— 6 1,2

Alterbidinium acutulum (Wilson 1967) Lentin & Williams 1985—————————————— 6 3

Andalusiella polymorpha (Malloy 1972) Lentin & Williams 1977————————————— 6 5

Andalusiella spicata (May 1980) Lentin & Williams 1981 ———————————~— 6 4, 6

Cerodinium pannuceum (Stanley 1965) Lentin & Williams 1987 ————————————— 6 7

Cerodinium striatum (Drugg 1967) Lentin & Williams 1987 ——-——-——-----—--—— 6 8

Cordosphaeridiumfibrospinosum Davey & Williams 1966 ———————————————— 6 9

Cribroperidinium Neal & Sarjeant 1962, emend. Helenes 1984 sp.———————————— 6 10 Diphyes recurvatumMay 1980—————————————————————————————————— 6 11

Exochosphaeridium Davey et al. 1966 sp.—————————————————————————— 6 12

Fromea Cookson & Eisenack 1958, emend. Yun 1981 spp. ———————————————— 6 13, 14

Lejeunecysta Artzner & Dorhofer 1978, emend. Bujak 1980 sp. —————————————— 7 18 Membranosphaera maastrictica Samoilovitch 1961 ————————————————————— 6 15

Odontochitina costata Alberti 1961————————————————————————————— 7 1

Operculodinium Wall 1967 spp. ——————————————————————————————— 6 16

Palaeohystrichophora infusorioides Deflandre 1935 ———————————————————— 7 2, 3

PalaeoperidiniumDeftandre 1934, emend. Sarjeant 1967 sp.———————————————— 7 4 Spiniferites Mantell 1850, emend. Sarjeant 1970 spp.———————————————————— 7 6

Spongodinium delitiense (Ehrenberg 1838) Deflandre 1936 ———————————————— 7 7

Tanyosphaeridium xanthiopyxides (Wetzel 1933) Stover & Evitt 1978—————————— 7 5

Tricodinium castanea (Deflandre 1935) Clark & Verdier 1967 ——————————————— 7 8, 9

Xenascus ceratioides (Deflandre 1937) Lentin & Williams 1973 ————————————— 7 19 Miscellaneous areoligeracean forms ————————————————————————————— 7 15-17, 21

Miscellaneous chorate forms (excluding Spiniferites spp.) ————————————————— 7 14 Small peridiniacean forms—————————————————————————————————— 7 10-13, 20 C10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

MILLHAVEN TEST HOLE Zone. Because of the presence of these taxa, Clarke and oth ers (1996) interpreted this sample as being Santonian in age The Millhaven test hole (33X048) was drilled by the and as belonging to Zone V (fig. 2). It should be noted that U.S. Geological Survey at lat 32°53'25" N., long 81°35'43" Praecursipollis plebius Tschudy apparently has not been W., near Sylvania, Burtons Ferry Landing 7.5-min quadran reported from the Atlantic Coastal Plain and is known only gle, Screven County, Ga. (fig. 1). The surface elevation is from a single sample of the Eutaw Formation in western 110 ft above sea level. Sixteen Upper Cretaceous samples Georgia (Tschudy, 1975). Sohl and others (1991) consid were examined for pollen and dinoflagellates from the depth ered the Eutaw Formation to be middle Coniacian to late interval of 1,212.0 to 680.8 ft (table 1). Stratigraphic occur (but not latest) Santonian in age in western Georgia. This rences of angiosperm pollen taxa in the productive samples formation age is used for the age range of Praecursipollis are shown in figure 3; many of these samples also contained plebius Tschudy shown in figure 5 and other range charts of the Cretaceous gymnosperm pollen genus Rugubivesiculites this paper that include this species. A very similar species, Pierce. Taxon occurrences of dinoflagellates in 10 samples Praecursipollis sp. A of Christopher (1979), has a range in are shown in figure 4. New Jersey from the base of the Complexiopollis exigua-Santalacites minor Zone to the lower part of the 1 Pseudoplicapollis cuneata-Semioculopollis verrucosa CAPE FEAR FORMATION Zone; thus, Praecursipollis sp. A has a range virtually iden tical to the range shown for Praecursipollis plebius Tschudy No palynological samples were studied from the Cape Fear Formation in the Millhaven core. in this paper. CP3B-1 and CP3B-6 of Wolfe (1976) are known from the uppermost part of the 1 Pseudoplicapollis cuneata-Semi MIDDENDORF FORMATION oculopollis verrucosa Zone, but they are not known to coex ist with Complexiopollis exigua Christopher, Momipites sp. SUBUNIT 2 I of Christopher (1979), and New genus D, sp. L of Christo pher (1979). CP3B-1 and CP3B-6 belong to the Holkopolle- Sample R4664 BA, from a 1,212.0-ft depth, is from nites complex, which is as yet poorly described and only subunit 2 of the Middendorf Formation. It contains only two partly illustrated. This complex is mainly developed in the useful angiosperm pollen taxa (fig. 3). Both of these range Campanian and Maastrichtian although it has its range base throughout Zone V (fig. 2), which is equivalent to the com in the Santonian (Christopher, 1982a). bined Complexiopollis exigua-Santalacites minor, PR-1 of Wolfe (1976), Proteacidites sp. aff. PR-3 of Pseudoplicapollis longiannulata-Plicapollis incisa, and Wolfe (1976), and CP3D-3 of Wolfe (1976) might be con IPseudoplicapollis cuneata-Semioculopollis verrucosa taminants, presumably from drilling mud, or they might Zones (fig. 2) of Coniacian, Santonian, and earliest Campa- nian age. The same sample contains rare dinoflagellate cysts have been misidentified. A more likely explanation for the of Palaeohystrichophora infusorioides Deflandre and other species range pattern in figure 5 is that sample R4664 CA peridiniacean forms, which suggests a marginal marine or contains a number of reworked taxa from the Coniacian and very nearshore marine environment. Coniacian to Santonian, but the sample is probably assign able to mid-Campanian Zone CA-4. Sample R4664 CA contains rare dinoflagellates of BLACK CREEK GROUP Palaeohystrichophora infusorioides Deflandre, other peri diniacean forms, and miscellaneous areoligeracean forms SUBUNIT 1 (fig. 4), suggesting a marginal marine or very nearshore marine environment. These dinoflagellate specimens might Sample R4664 CA, from a depth of 1,124.3 to 1,124.7 be reworked. However, this possibility is unlikely because ft in the Millhaven test hole, is from subunit 1 of the Black (1) the specimens are fragile and would not withstand Creek Group. Pollen taxa occurrences in this sample are reworking while remaining in a fair state of preservation, shown in figure 5. Six species are not known to range and (2) formations from which they might be reworked higher, or they barely range higher, than the top of (Cape Fear and Middendorf) are entirely or nearly entirely the 1 Pseudoplicapollis cuneata-Semioculopollis verrucosa nonmarine. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C11

\J C* ^ : °5 T "g O) Is 0 5" ^ LLI ^ s- a •)" ! CO ^- « T ~ it. ) 0^ r > ^- ( > £ j T S J i * i ! § 1 5 c 3 co -5 t 5h L H 05 v 1 0 £ o co .£ j i ^ "i ' ^ r 1 j 0 w LLI ?): •'H 3 i Cj ! 2- X j -o -— ^ •;; = c 5 p i i i5 5 *c1 i 3. 3 "c n i ^ 5 5 5 C 5 g X : ex 1 = £ f 8-1 s ~ !co 1" 3 " H •>- ah .^ _^ w o> TO IjU "o ^ ^ ^^ o> ^ ~^rv-^-' 0 SAMPLESOFSERIR4664 5 - (j ? S : S5 u J si D •r . ft 1 « * - T > '$ 2 TO M § ""^ < 33. ® r£ ^ •>- $ *= r\ £ ** i !i c1 «5 1£ 5 1 ' 0 J D a 0 >2) Z. "S|lf d3 *d«l^« -I 81 «ls. i c 1 I I! h ' J >c= -^~ P > co » 0 3" * 13 C » •! Holkopollenitesspp. %o3ii;S'*-t to Q (D -^ O co c*trO •*-" S c .0 »" * : < : C 3 I' ] - C -^ ^0 Q) ^ fc*~**--C> O O > ^^ i a2 i h 1 *o S 0 " . c 3 5 - < ^.S2 tS-G*Q(bo"£Q) -2 ^ ^ fn" *£ CO 5 1i ih i"3 *3 .C , 5 l! 3 C" n: cM5S - Q u- C hy: Q:* H; C) tII!!N: c_) D :-2§§b$£i2$o5z£o§'-j£oo c > A o o i o o

STEEL GA 41 0 4> • • O CREEK FM. 800 (PART)

FE o A 0 , , , 4> • • DA,CD ( ) 0 ( CC i A CO 1- z

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1100-

CA 4 i C5 0 (5 CD C5 3 D < > 4 1 1 I 3 H Z

MIDDEN- OJ

DORF | 15 1200 FM. (PART) 1 CO

Figure 3. Chart showing pollen taxa occurrences in 11 samples A = aff., meaning the specimens observed were similar to the taxon between 1,212.0 and 733.2 ft in the Millhaven core, Screven listed but probably belong to a different species; C = cf., meaning County, Ga. Solid circles indicate that the identification of the that the specimens are similar to and may well belong to the taxon specimens was checked by R.A. Christopher from listed; P indicates that the specimens probably belong to the taxon photomicrographs provided by the senior author; hollow circles listed; Q indicates that identification of the taxon was questionable, indicate that the identification of the specimens was not so checked; uncertain. Depths are in feet below land surface. FM., Formation. C12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

VO £ Q. 'usorioide Q. « pinosum CO CO CO o> £ o ! r- E to | •c CO ca o>

miscellaneousareoliger Spongodiniumdelitiens Palaeohystrichophoraii smallperidiniaceanfor Alisogymnium-Dinogymr Cerodiniumpannuceun Tanyosphaeridiumxant Cordosphaeridiumfibro Operculodiniumspp. Andalusiellapolymorph choralemiscellaneous Andalusiellaspicata Xenascusceratioides Palaeoperidiniumsp. Cerodiniumstriatum Cribroperidiniumsp. Diphyesrecurvatum Lejeunecystasp. Q. Q. CO a. K $ 1

700 - STEEL CREEK - CF No Dinocysls FORMATION - FG

800 - FE No Dinocysls CD t t h CC + * + SUB- UNIT 3 900 - CB o o FD •

BLACK 1000 - CREEK SUB- GROUP UNIT 2 - BB

1100 - - CA SUB- UNIT 1

1200 - SUB- - BA UNIT 2

MIDDEN- DORF 1300 - FM. SUB- UNIT 1

CAPE FEAR FM.

Figure 4. Chart showing dinoflagellate taxa occurrences in 10 samples between 1,212.0 and 680.8 ft in the Millhaven core, Screven County, Ga. Depths are in feet below land surface. FM., Formation. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C13

lj i Complexiopollisexigua cL c POLLEN W ASSEMBLAGE-ZONES a. >? £ ^ SUB- OF CHRISTOPHER i 1 1 o CO CO CO ZONE ZONE (1979)

NO DAT/V < i- CA-6/ E MA-1 - o t\\ cc I I J m1 CA-5 3

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1PSEUDOPLICAPOLLIS CUNEATA- |SANTON.-CONIACIAN SEMIOCULOPOLL1S VERRUCOSA

PSEUDOPLICAPOLLIS LONGIANNULATA- NO DAT \ PLICAPOLLIS INCISA

COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR

fe^KBftE 1

Figure 5. Chart showing known stratigraphic ranges of pollen taxa in sample R4664 CA, subunit 1 of the Black Creek Group, from 1,124.3-1,124.7 ft in the Millhaven core, Screven County, Ga. The known range shown for N20-2 of R.A. Christopher (unpublished) is from Christopher (written commun., 1996). The identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. Full names of taxa are in figure 3 and table 4. C14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

SUBUNIT 2 POLLEN ZONATION OF WOLFE Pollen grains and dinoflagellates were examined from (1976) AND LITWIN two samples of subunit 2 of the Black Creek Group in the AND OTHERS Millhaven core. They are R4664 BB and R4664 FD (figs. 3, (1993) 4). Pollen taxa occurrences in sample R4664 BB, from a 1,029.5-ft depth, are shown in figure 6. The stratigraphic ranges are not very informative except to indicate that the age of the sample is probably late Campanian or Maastricht- ian. However, Bukry (this volume, chap. D) reports that on the basis of calcareous nannofossils the interval between 1,077.0 and 968.0 ft is late Campanian (Zone CC 22) in age. Sample R4664 FD, from a depth of 941.7 to 941.9 ft, contains mainly long-ranging pollen taxa (fig. 7). Interpreta tion of the stratigraphic ranges is complicated by the fact that the specimen identified as cf. ND-2 only probably belongs to species ND-2 of Wolfe (1976), and the identifica tion of species PR-1 of Wolfe (1976) was even more tenu ous. However, like the underlying sample R4664 BB, this sample cannot be older than late Campanian; therefore, the specimen of New genus D, sp. H of Christopher (1979) is reworked or was misidentified, or its range should be extended upward. Dinoflagellates are moderately abundant and diverse in samples R4664 BB and FD (1,029.5 and 941.7-941.9 ft, respectively; fig. 4). Important species include Andalusiella spicata (May) Lentin & Williams, Cerodinium striatum (Drugg) Lentin & Williams, Cerodinium pannuceum (Stan ley) Lentin & Williams, Palaeohystrichophora infusorioides Deflandre, and Xenascus ceratioides (Deflandre) Lentin & Williams. The assemblage indicates correlation with the Mount Laurel Formation in New Jersey. This is because the first two species have their lowest occurrences in the Mount Figure 6. Chart showing known stratigraphic ranges of pollen Laurel Formation and the last three species have their high taxa in sample R4664 BB, subunit 2 of the Black Creek Group, est occurrences near the top of the Mount Laurel Formation from 1,029.5 ft in the Millhaven core, Screven County, Ga. The (May, 1980). As previously stated, we consider the Mount identification of the taxon followed by an asterisk was checked by Laurel Formation to be upper Campanian. However, late R.A. Christopher from photomicrographs provided by the senior author; therefore, this taxon is of greater significance than the Campanian calcareous nannofossils were only found as other. Full names of taxa are in figure 3 and table 4. The question high as 968.0 ft (Bukry, this volume, chap. D). Therefore, mark indicates that the youngest age of the taxon is uncertain. the possibility cannot be excluded that some of the stratigraphically highest occurrences of diverse dinoflagellate assemblages in the Millhaven core (as well as in the Girard and Thompson Oak cores) might be correlative with the uppermost Campanian part of the Mount Laurel-Navesink unconformity (fig. 2), that is, slightly younger than the pre served Mount Laurel Formation itself. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C15

I d. POLLEN '0 •= C S u ZONATION c ^ O V OF WOLFE 3 ° •- (1976) j AND LITWIN i 5 i ^ .£ ^ M AND OTHERS POLLEN ^' Z ,_ g 5 ^ LU g (1993) ASSEMBLAGE-ZONES 1 ^ re -^ ct >? £ ^ SUB- OF CHRISTOPHER 2: 0 51 i= c- CO CO CO ZONE ZONE (1979) /

•z. NO DATA B P CA-6/ MA-1 — O A cc

• H CA-5 B s NO DATA CO Z O cc CA-5 LU LU QL A < QL 1 QL —^ CA-4 LUtr *E o o B CA-3 A

CA-2 B

CA-2? A?

Z32HZ1 o 7PSEUDOPLICAPOLLIS CUNEATA- SEM1OCULOPOLLIS VERRUCOSA Z CO PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA Z o COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR Z o o

Figure 7. Chart showing known stratigraphic ranges of pollen taxa in sample R4664 FD, subunit 2 of the Black Creek Group, from 941.7-941.9 ft in the Millhaven core, Screven County, Ga. The identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. The stratigraphic range shown for species cf. ND-2 is the known range of ND-2 of Wolfe (1976). The identification of species PR-1 of Wolfe (1976) was uncertain. Full names of taxa are in figure 3 and table 4. C16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

SUBUNIT 3 These three samples contain many taxa that were not found to range lower in the Millhaven core section. These Pollen grains and dinoflagellates were examined from pollen taxa include several reworked forms from the Santo- two samples of subunit 3 of the Black Creek Group in the nian and lower Campanian, but the bulk of the evidence Millhaven core. They are R4664 CB and R4664 CC (figs. 3, points to a Campanian or Maastrichtian age. The apparent 4). presence of CP3E-1 of Wolfe (1976) and cf. MPH-1 of Sample R4664 CB from a depth of 913.8-914.2 ft has Wolfe (1976) suggests an assignment to Zone CA-5, of mid only sparse pollen grains that include only a few taxa (fig. dle to late Campanian age. However, the specimen of cf. 3). The only useful species, Lanagiopollis cribellatus MPH-1 may have been misidentified or may be reworked, (Srivastava) Frederiksen, ranges from mid-Campanian Zone and CP3E-1 might be observed to range up into the early CA-4 into the Paleocene. Maastrichtian if strata of that age are found preserved in cer Sample R4664 CC, from 849.3-849.6 ft, contains so tain parts of the coastal plain. The critical taxon in these few (fig. 3) and such long-ranging pollen taxa that little can samples is a new species, Momipites n. sp. 1 (pi. 1, figs. 6, 7, be said about its age. 10-12), known only from the Maastrichtian (R.A. Christo The dinoflagellate assemblage in sample R4664 CB of pher, written commun., 1996). However, the species might subunit 3 (913.8-914.2 ft; fig. 4) is virtually identical to the possibly be determined to range down into the uppermost assemblage in the sample below (R4664 FD at 941.7-941.9 Campanian if strata of that age are locally found to be pre ft) in subunit 2. Important species include Andalusiella spi- served. Furthermore, the pollen assemblage in sample cata (May) Lentin & Williams, Cerodinium striatum R4664 DA includes a specimen of Interporopollenites turgi- (Drugg) Lentin & Williams, Palaeohystrichophora infusori- dus Tschudy (pi. 2, fig. 2), which apparently has previously oides Deflandre, and Xenascus ceratioides (Deflandre) Len been known only from the lower Paleocene (Tschudy, tin & Williams. Here again, the assemblage is late 1975). This specimen may represent contamination from Campanian, correlative with the Mount Laurel Formation in drilling mud, but it appears more likely that this occurrence New Jersey. demonstrates that the species actually ranges, in the form of Sample R4664 CC (849.3-849.6 ft) has a less diverse rare specimens, down into the Upper Cretaceous. If this is assemblage but contains the highest occurrence of Palaeo so, then the presence of Interporopollenites turgidus hystrichophora infusorioides Deflandre. The highest occur Tschudy would also suggest that the samples are Maas rence of P. infusorioides Deflandre marks the top of Koch trichtian. In summary, because reworking and misidentifica- and Olsson's (1977) P. infusorioides Zone, which we now tion are more likely than contamination from uphole, sam consider to correlate approximately with the Campa- ples R4664 CD, DA, and FE are most likely Maastrichtian nian-Maastrichtian boundary. in age. Sample R4664 CD, from a depth of 830.3-830.5 ft in the Steel Creek Formation, contains a rather sparse STEEL CREEK FORMATION dinoflagellate assemblage. The presence of Spongodinium delitiense (Ehrenberg) Deflandre, which has its lowest Ten samples of the Steel Creek Formation from the Millhaven test hole were examined for pollen and occurrence in the upper part of the Mount Laurel Formation dinoflagellates. Three samples were barren of both pollen in New Jersey (May, 1980), indicates that the sample is late and dinoflagellates (table 1): R4664 FF, CE, and CG. A Campanian or Maastrichtian. fourth sample—R4664 GB—contains practically no pollen Sample R4664 FE, from 824.1-824.4 ft, does not con and only late Paleocene dinoflagellates, which are clearly tain dinoflagellates; sample R4664 DA, from 829.5-829.8 contaminants from uphole. The six samples providing bio- ft, was not examined for these fossils. stratigraphic information are discussed below. In summary, the Campanian-Maastrichtian boundary Figure 8 displays stratigraphic ranges of pollen taxa in in the Millhaven core appears to be between 849.3-849.6 three Steel Creek samples from between depths of 830.5 and 830.3-830.5 ft, apparently coinciding with the bound and 824.1 ft in the Millhaven test hole: ary between the Black Creek Group and the Steel Creek Sample Depth below land Formation at 839.0 ft. This is because the last occurrence of surface, in feet Palaeohystrichophora infusorioides Deflandre is at 849.3- R4664 FE 824.1-824.4 849.6 ft and the species is not known to range higher than R4664 DA 829.5-829.8 the Campanian (as the Campanian-Maastrichtian boundary R4664 CD 830.3-830.5 is defined in Burnett, 1996), and the first appearance of PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C17

Q. O

POLLEN ZONATION OF WOLFE (1976) .CDCO £« AND LITWIN CO •S- ^ M AND OTHERS POLLEN l. LJJ Q co co H y O (1993) ASSEMBLAGE-ZONES D. Q. 8 ± Q_ Q- 0 0 CL Z O £ S P* SUB- OF CHRISTOPHER C/) C/) C/) ZONE ZONE (1979)

NO DATA

CA-5

CA-4

CA-2

-?• 1PSEUDOPLICAPOLLIS CUNEATA- SEMIOCULOPOLLIS VERRUCOSA

PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA

COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR

Figure 8. Chart showing known stratigraphic ranges of pollen taxa in three samples (R4664 CD, DA, and FE) from the Steel Creek Formation between 830.5 and 824.1 ft in the Millhaven core, Screven County, Ga. The identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. The identification of CP3E-1 of Wolfe (1976) and MPH-1 of Wolfe (1976) was only probable; the range lines show the known stratigraphic ranges of the species themselves. Full names of taxa are in figure 3 and table 4. CIS GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Maastrichtian pollen species Momipites n. sp. 1 is at 830.3- 830.5 ft. Sample R4664 GA, from a depth of 769.0 to 769.3 ft, POLLEN ZONATION contains pollen species CP3F-1 of Wolfe (1976), not OF WOLFE (1976) thought to range higher than the mid-Campanian, as well as AND LITWIN Casuarinidites sp. A of Frederiksen and Christopher (1978) ^ „. AND OTHERS POLLEN H y CD '1993' Q_ CQ and Lanagiopollis cribellatus (Srivastava) Frederiksen, ASSEMBLAGE-ZONES £ g £ SUB- OF CHRISTOPHER o o which probably range from about the mid-Campanian to CO CO CO ZONE ZONE (1979) near the top or above the top of the Cretaceous (fig. 9). NO DATA Underlying samples from the Steel Creek Formation are very probably Maastrichtian; therefore, the specimen of CP3F-1 of Wolfe (1976) is presumably reworked. One spec imen was found in sample R4664 GA that resembles Tripo- rate type 4 of Christopher (1979), which is known only from one sample from the middle of the Magothy Formation near the Coniacian-Santonian boundary of New Jersey. Either the specimen in the Millhaven core represents a different spe cies, or the species (species group?) actually ranges from the Santonian up to the Maastrichtian, or else the specimen is reworked from older strata. Sample R4664 GA lacks dinoflagellates. Sample R4664 FG, from a depth of 755.0 to 755.3 ft, does not contain any known Cretaceous pollen grains. Instead, it has the lower Tertiary taxa Sparganiaceaepolleni- tes sp., Plicatopollis triradiatus (Nichols) Frederiksen & Christopher, and Momipites-Plicatopollis-Platycaryapolle- nites complex of Frederiksen (1979). These specimens no 7PSEUDOPLICAPOLLIS CUNEATA- doubt represent contamination of the sample by drilling SEM1OCULOPOLLIS VERRUCOSA mud. This sample also contains sparse dinoflagellates (fig. PSEUDOPLICAPOLLIS LONGIANNULATA- 4) that may be either indigenous (Late Cretaceous), indicat PLICAPOLL/S INCISA ing at least a marginally marine environment of deposition, COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR or may be Tertiary specimens representing contamination from uphole. Sample R4664 CF, from a depth of 733.2 to 733.3 ft, Figure 9. Chart showing known stratigraphic ranges of pollen apparently is late Campanian or early Maastrichtian in age taxa in sample R4664 GA, Steel Creek Formation, from 769.0- according to the ranges of its pollen taxa (fig. 10). Because 769.3 ft in the Millhaven core, Screven County, Ga. The of the apparent Maastrichtian age of samples lower in the identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior section (fig. 8), this is also probably Maastrichtian. This author; therefore, these taxa are of greater significance than the sample lacked dinoflagellates. others. Full names of taxa are in figure 3 and table 4. A range line for C3C-1 of Wolfe (1976) is not shown because the specimen found is only similar to but probably not the same species as C3C-1. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C19

POLLEN •2 2ONATION OF WOLFE (1976) AND LITWIN 3 CO mAND °THERS POLLEN hj. in H U (D (1993) ASSEMBLAGE-ZONES CC CC CO CC < CI1D CL CL >- LLJ h- SUB~ OF CHRISTOPHER CO CO CO ZONE ZONE (1979)

NO DATA

CA-5

CA-4

CA-3

CA-2

CA-2?

7PSEUDOPLICAPOLLIS CUNEATA- SEMIOCULOPOLL1S VEFIFtUCOSA

PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA

COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR

Figure 10. Chart showing known stratigraphic ranges of pollen taxa in sample R4664 CF, Steel Creek Formation, from 733.2-733.3 ft in the Millhaven core, Screven County, Ga. Full names of taxa are in figure 3 and table 4. C20 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

GIRARD TEST HOLE

The U.S. Geological Survey drilled the Girard test hole (32Y020) in southern Burke County at the lookout tower on Griffins Landing Road, 2 miles north of the town of Girard, at lat 33°03'54" N., long 81°43'13" W., Girard 7.5-min o quadrangle (fig. 1). The surface elevation is 250 ft above sea level. Nineteen Upper Cretaceous samples from this core were examined for palynomorphs (table 1). Three of these were scanned in detail for pollen (fig. 11), and four samples were scanned in detail for dinoflagellates (fig. 12).

— r» c 0 «3 05 :3 a? o> t5 «• T- : T- -' a15 >- I " ^ ^ '-£ CX i CAPE FEAR FORMATION D ^ ? s* ci °3 Jr?^ s- D 0 I i0 C ° 0 LL 5 S•. 50 O O * 7 h Brevicolporites: N20-12R.A.of _ « !l M CP3D-3ofWo No palynological samples were studied from the Cape • H--> 1 j-- O W il 5 j O LU - 1 Fear Formation in the Girard core. _l _l 5 T.. "c S T. - c o a. c i! i- u a ' c 1 5 : c" X ^ ? ° i{5 C 5 g LU b1- < _a> >n nucS a O _l w 5 2: cs!: <. ) C.5 S

MIDDENDORF FORMATION DOR^ C) ( • o •

800- BLACK SUB- UNIT CREEK 2 SUBUNIT 1 GROUP 900 (PART) sulF UNIT Sample R4705 AA, from a depth of 1,138.0 to 1,139.0 1

ft in the Girard core, is from subunit 1 of the Middendorf MIDDEN SUB- 1000- UNIT -BA c ) Ci ci

LLI "5a £ Q. E CO 9- s ca c w c to ."§.u m o c o to E »$ £ $ £«* & Palaeohystrichophorainfu ^ &II gl - t|a Membranosphaeramaast choratefomiscellaneous coSSs -g^g-Q-Eg^S b S Exochosphaeridiumsp. LU Z h- Tricodiniumcastaneal LU 3 LL LL SMU unit* 8 - 0 co LU *3ig«* 8 lii3«§j O LU ?Si.i3«s|?1^3l? I -1 -1 m 8. a 1. . §S«i8S--iS.SSS8 CL ° % £ iihig!« |!|ii| Q Ij CO illa^l«3*aS^^8

STEEL CREEK 600 - FM. (part)

SUB- UNIT 3 700 - - BH No Dinocysts — BGDf^ ~

BLACK - CE o <» 0 0 0 800 - CREEK GROUP SUB- UNIT 2 TR 0 0 -

RC - BE No Dinocysts 900 - - DD No Dinocysts SUB- - BD No Dinocysts - UNIT 1

- DC No 1000 - SUB- Dinocysts UNIT 2 - DB, BA No Dinocysts - AC No Dinocysts MIDDEN- - DA No Dinocysts DORF - AB No Dinocysts FM. 1100 - SUB- UNIT 1 - AA No Dinocysts _

CAPE 1200 - FEAR FM. (part)

Figure 12. Chart showing dinoflagellate taxa occurrences in 15 samples between 1,139.0 and 720.3 ft in the; Girard core, Burke County, Ga. Depths are in feet below land surface. FM., Formation. Four samples were scanned in detail for dinoflagellates. Question marks within range lines indicate uncertainty of identification. C22 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

POLLEN w POLLEN ZONATION Q" ZONATION OF WOLFE w OF WOLFE Complexiopollisabdi———————————————————— (1976) § (1976) AND LITWIN D) ^~ ^ AND LITWIN CP3F-1* 2 OT AND OTHERS POLLEN LJJ cp C ^ OT AND OTHERS POLLEN H y O (1993) ASSEMBLAGE-ZONES CD Q. 6 Q |£ W <3 (1993) ASSEMBLAGE-ZONES £ £ j5 SUB- OF CHRISTOPHER Z O Z C > £ j5 SUB- OF CHRISTOPHER CO CO CO ZONE ZONE (1979) CO CO CO ZONE ZONE (1979) •MvSFmnm^mm** 3Myiiiisigii»»H NO DATA ? : NO DATA Z < B I- CA-6/ B H CA-6/ I MA-1 — MA-1 - O A o A rr MAASTF &%$a i 1%m 1

CA-5 B CA-5 B

1i NO DATA m 81 1 C/3 i D •z. i B CRETACEOUS E3 O cc < CA-5 < CA-5 - LLJ LLJ UPPER A QL A Q. I D | CA-4 1 CA-4 cc < < 0 O 0 B B CA-3 CA-3 - A A

CA-2 B CA-2 B ~K A" E CA-2? A? CA-2? \1 -?- z CA-1 I ? PSEUDOPLICAPOLLIS CUNEATA- 7 PSEUDOPLICAPOLLIS CUNEATA- O SEMIOCULOPOLLIS VERRUCOSA o SEM/OCULOPOLLIS VERRUCOSA z < < C/3 PSEUDOPLICAPOLLIS LONGIANNULATA- C/3 PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA NO DATA PLICAPOLLIS INCISA Z < < o COMPLEXIOPOLLIS EXIGUA- COMPLEXIOPOLLIS EXIGUA- < SANTALACITES MINOR i SANTALACITES MINOR z o g 0

Figure 13. Chart showing known stratigraphic ranges of pollen Figure 14. Chart showing known stratigraphic ranges of pollen taxa in sample R4705 AA, subunit 1 of the Middendorf taxa in sample R4705 BA, subunit 2 of the Middendorf Formation, Formation, from 1,138.0-1,139.0 ft in the Girard core, Burke from 1,012.0-1,012.3 ft in the Girard core, Burke County, Ga. The County, Ga. Taxa followed by an asterisk indicate that identification of the taxon followed by an asterisk was checked by identification of the specimens was checked by R.A. Christopher R.A. Christopher from photomicrographs provided by the senior from photomicrographs provided by the senior author. Full names author; therefore, this taxon is of greater significance than the of taxa are in figure 11 and table 4. Question marks indicate that others. Full names of taxa are in figure 11 and table 4. the youngest age of the taxon is uncertain. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C23

BLACK CREEK GROUP POLLEN ZONATION OF WOLFE The lowest marine palynomorphs in the Black Creek (1976) AND LITWIN Group in the Girard core were found at 868.5-868.7 ft, in AND OTHERS subunit 2, and the presence and absence pattern of dino- (1993) DCF <° SUB- flagellate occurrences (fig. 12) suggests nonmarine LJJ CO CO ZONE ZONE conditions in subunit 1 of the Black Creek Group, then marine conditions in subunit 2, then nonmarine deposition in subunit 3 of the Black Creek. The dinoflagellate-bearing assemblages in the Girard core are not as rich but contain many of the same taxa and are the same age as samples from subunit 2 and the lower part of subunit 3 of the Black Creek Group in the Millhaven core. The taxa found in Black Creek samples from both cores are Palaeohystrichophora infusorioides Deflandre, Xenascus ceratioides (Deflandre) Lentin & Williams, Cordosphaeridium fibrospinosum Davey & Williams, and Andalusiella spicata (May) Lentin & Williams. In the Millhaven core, these assemblages came from strata assignable in part to late Campanian calcareous nannofossil Zone CC 22 (Bukry, this volume, chap. D), and the dinoflagellate assemblages were correlated with those from the upper Campanian Mount Laurel Formation of New Jersey. Most pollen assemblages from the Black Creek of the Girard core are sparse and not age diagnostic. However, sample R4705 BG, from 738.3 to 738.6 ft (subunit 2 of the Black Creek Group), had two useful pollen taxa (fig. 15), and the overlap of the ranges of these taxa suggests a middle to late Campanian age somewhere within Zone CA-4 or Zone CA-5. As noted above, dinoflagellates from this sam ple suggest a late Campanian age correlative with the upper part of pollen Zone CA-5.

CA-4 STEEL CREEK FORMATION

No palynological samples were studied from the Steel CA-3 Creek Formation in the Girard core.

CA-2 THOMPSON OAK TEST HOLE

The Thompson Oak test hole was drilled by the Geor CA-2? A? gia Geologic Survey at lat 33°10'42" N., long 81°47'10" W., Shell Bluff Landing 7.5-min quadrangle, Burke County, Ga. Figure 15. Chart showing known stratigraphic ranges of (fig. 1). The surface elevation is 240 ft above sea level. Two pollen taxa in sample R4705 BG, subunit 2 of the Black samples were examined from this core. Creek Group, from 738.3-738.6 ft in the Girard core, Burke County, Ga. Not shown is species N20-12 of R.A. Christopher (unpub.), which has a very long stratigraphic range from Zone V (fig. 2) to the Maastrichtian (R.A. Christopher, written commun., 1996). The identification of the taxon followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, this taxon is of greater significance than the other. Full names of taxa are in figure 11 and table 4. C24 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

BLACK CREEK GROUP

Two samples from the Black Creek Group in the infusorioides forrreracean Thompson Oak core were examined for dinoflagellates. The lower sample (R4836 A, 561.0 ft depth) is from a kaolinitic, CO o lignitic, micaceous sand. It contains only three dinoflagel- r-n 1-J tn late specimens that do not appear to be marine. The upper areolkmiscellaneous ceratioidetXenascus Palaeohystrichophora Cerodiniumpannuce spicataAndalusiella Operculodiniumspp. sample (R4836 B, 505.0 ft depth) is from a sandy, mica peridiniaceansmall ceous, lignitic kaolin and contains a sparse assemblage sim o o ilar to that of samples R4664 BB to CB (from subunit 2 and 3 the lowermost part of subunit 3 of the Black Creek Group) o in the Millhaven core, that is, Palaeohystrichophom infusor CO ioides Deflandre(?), Xenascus ceratioides (Deflandre) Len- tin & Williams, and Andalusiella spicata (May) Lentin & STEEL CR FM. (part) Williams (fig. 16). These dinoflagellate taxa indicate a near- 400 - shore marine to normal marine environment of deposition and a late Campanian age.

MILLERS POND TEST HOLE 500 - - B BLACK The Millers Pond test hole was drilled by the Georgia CREEK Geologic Survey (Burke 2, GGS-3758) near Shell Bluff GROUP - A Landing on the Savannah River, lat 33°13'48" N., long 81°52'44" W, McBean 7.5-min quadrangle, Burke County, 600 - Ga. (fig. 1). The surface elevation is 245 ft above sea level. Clarke and others (1994) provided a lithologic description of the cored section.

Fifteen samples were collected from Cretaceous strata 700 - in this core (table 1) from the depth interval of 852.0 to 282.0 ft. Only four contained useful pollen assemblages MIDDEN- (fig. 17), and none of the samples contained marine DORF palynomorphs. FM. 800 -

CAPE FEAR FORMATION

CAPE Christopher and others (1979) examined samples from FEAR the Cape Fear Formation of North Carolina and concluded, 900 - FM. on the basis of the pollen flora, that the Cape Fear Forma (part) tion could be assigned to undifferentiated pollen Zone V, which is approximately equivalent to the combined Com- Figure 16. Chart showing dinoflagellate taxa occurrences in plexiopollis exigua-Santalacites minor, Pseudoplicapollis two samples from 561.0 and 505.0 ft, respectively (Black Creek longiannulata-Plicapollis incisa, and IPseudoplicapollis Group), in the Thompson Oak core, Burke County, Ga. Depths cuneata-Semioculopollis verrucosa Zones of Coniacian to are in feet below land surface. FM., Formation. Full names of earliest Campanian age (fig. 2). taxa are in table 5. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C25

£35 03 03 .|

° _ O Q £ § x co

.<2 .2 .fo O) z | w lilt !alllll!|i !!nl'll 0^5 1 1 1 ^ —1 _| ^^^'r\""sJS^^^Qi^ :sRD>"o"OD) <"> n Q. "^ 1~ ^ O ^ 'S g] f 2 SEE||cE^EEE|fe5225§S^3^<2^ T'"S Q i] co ooo^^^otooo^^zSSziSix^cSooz^zi^

BLACK 600- CREEK GR h° P - DORF 700- FM. CAPE 800- -c • c } C3 C5 * C3 6 «» C) > « » ( 5 FEAR FM. D ft f

Figure 17. Chart showing pollen taxa occurrences in four samples between 832.0 and 517.0 ft in the Millers Pond core, Burke County, Ga. Solid circles indicate that the identification of the specimens was checked by R.A. Christopher from photomicrographs provided by the senior author; hollow circles indicate that the identification of the specimens was not so checked; C = cf., meaning that the specimens are similar to and may well belong to the taxon listed; P indicates that the specimens probably belong to the taxon listed. Depths are in feet below land surface. GR., Group; FM., Formation.

Sample R4581 B, from a depth of 827.0 to 832.0 ft in also the case with Praecursipollis plebius Tschudy (dis the Millers Pond core, contains pollen taxa whose ranges cussed under sample R4664 CA, Black Creek Group of the suggest assignment to the combined Complexiopollis Millhaven core). Clarke and others (1994, 1996) and Leeth exigua-Santalacites minor, Pseudoplicapollis longiannu- and others (1996) considered the Eutaw Formation of the lata-Plicapollis incisa, and 1 Pseudoplicapollis cuneata- eastern Gulf Coast to be correlative with the Middendorf Semioculopollis verrucosa Zones (figs. 2, 18; the range of Formation, not with the Cape Fear Formation, of the South Momipites sp. I of Christopher (1979) is difficult to evaluate ern Atlantic Coastal Plain. As an alternative interpretation, because the identification of this species has not been veri Prowell, Christopher, and others (1985) correlated the Cape fied). However, sample R4581 C, from a depth of 797.0 to Fear Formation with the lower half of the Eutaw Formation, 802.0 ft, can be narrowed to the Complexiopollis and the Middendorf Formation with the upper half of the exigua-Santalacites minor and Pseudoplicapollis longian- Eutaw Formation. nulata-Plicapollis incisa Zones (fig. 19) and most likely The lack of both marine palynomorphs (dinoflagel- belongs to the Complexiopollis exigua-Santalacites minor lates, acritarchs) and microforaminiferal linings in samples Zone of Coniacian age. Therefore, the underlying sample R4581 B and R4581 C suggests a nonmarine environment R4581 B would also belong to this zone. The occurrence of of deposition for the Cape Fear Formation. New Genus A of Tschudy (1975) is interesting, as it was Two additional samples from the Cape Fear Formation, previously known only from a single sample of the Eutaw from depths of 847.0-852.0 and 778.0 ft, were barren of Formation in western Georgia (Tschudy, 1975), which was palynomorphs. C26 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

UJ POLLEN Q. Q. Q. ZONATION C/> ,5 3 .co W CO O OF WOLFE .w .CO i1 .CO « 'g i .£2 ^ (1976) vfc AND LITWIN a 'n ^ I ,O co -S-r\ co I AND OTHERS POLLEN o CO ^j ^ •S ij (1993) ASSEMBLAGE-ZONES o o -§• -S E E E S c 5 SUB- OF CHRISTOPHER o o CO CO CO CO ZONE ZONE (1979) O O i i 1 CO CA-4

CA-3 B NVINVdlAIVOc A NO DATA CA-2 B "A CRETACEOUS aaddn CA-2? A?

7PSEUDOPLICAPOLLIS CUNEATA- NVIOVINOO"NO1NVS- SEMIOCULOPOLLIS VERRUCOSA

PSEUDOPL/CAPOLLIS LONGIANNULATA- NO DATA PL/CAPOLLIS INC/SA

COMPLEXIOPOLL/S EXIGUA- SANTALACITES MINOR

Figure 18. Chart showing known stratigraphic ranges of pollen taxa in sample R4581 B, Cape Fear Formation, from 827.0-832.0 ft in the Millers Pond core, Burke County, Ga. The identification of taxa followed by an asterisk was checked by R. A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. Full names of taxa are in figure 17 and table 4.

MIDDENDORF FORMATION is thought to be uppermost Santonian or lowermost Campa- nian, suggesting that Casuarinidites sp. A of Frederiksen No productive palynological samples were studied and Christopher (1978) has its range base near the base of from the Middendorf Formation in the Millers Pond core. the Campanian. In summary, Millers Pond sample R4581 G may be latest Santonian or earliest Campanian like the Girard sample, or it may be younger. BLACK CREEK GROUP Sample R4581 I, from 517.0 ft, contains taxa having a Sample R4581 G, from 578.0 ft, contained only rare great variety of known stratigraphic ranges (fig. 20). Prae- angiosperm pollen grains; the only useful pollen species cursipollis plebius Tschudy is probably reworked. If NF-1 (whose identification is probably correct) was Casuarini- and CP3B-1 are reworked or misidentified, the other taxa dites sp. A of Frederiksen and Christopher (1978). In the would suggest a middle to late Campanian age within Zones Middle Atlantic States, this species has a known range base CA-4 or CA-5. The absence of marine dinoflagellates and in the mid-Campanian (see fig. 14). However, sample microforaminiferal linings in this sample (as in all Creta R4705 BA, from the Middendorf Formation of the Girard ceous samples from the Millers Pond core) indicates a non- core, also contains this species (fig. 14). This Girard sample marine environment of deposition. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C27

Q. CO Q CO X POLLEN § C I Q. Q. d. ZONATION CD 1 X Q. Q" OF WOLFE .CO .co ,co ^ 1"o 1 (1976) "o d. •£ "o Q. to 8- AND LITWIN 8- o ^i §- co -S- C 1'i I .CO ^ w AND OTHERS POLLEN Qi CO 05 CD "o 1 CT CT 1 H y o <1993) ASSEMBLAGE-ZONES Q. :§. B c^_ P Qi | CVJ 1 1 ^ £ H SUB- OF CHRISTOPHER I o 5 CD CD £ | WWW ZONE ZONE (1979) a § £ a z O- £

CA-4

z CA-3 — A NO DATA n CA-2 B CO O k 0 us UJ CA-2? A? 0 Q. D IT, CA-1 I 7PSEUDOPLICAPOLLIS CUNEATA- cc SEMIOCULOPOLLIS VERRUCOSA u Rz CO PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA o COMPLEXIOPOLLIS EXIGUA- SANTALACITES MINOR z o o

Figure 19. Chart showing known stratigraphic ranges of pollen taxa in sample R4581 C, Cape Fear Formation, from 797.0-802.0 ft in the Millers Pond core, Burke County, Ga. The known range shown for Porocolpopollenites n. sp. 1 is from Christopher (written commun., 1996). The identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. Full names of taxa are in figure 17 and table 4. C28 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

POLLEN ZONATION OF WOLFE O (1976) .Q- AND LITWIN g eo mAND OTHERS POLLEN O CM £ < T S «? £ UJ O < 1993> ASSEMBLAGE-ZONES 5 m LL a. co Q. Q. Q. O Z O Z O Z £ £ £ SUB- OF CHRISTOPHER C/D CO CO ZONE ZONE (1979)

NO DATA

CA-5

CA-4

CA-3

CA-2

1PSEUDOPLICAPOLLIS CUNEATA- SEMIOCULOPOLLIS VERRUCOSA

PSEUDOPLICAPOLLIS LONGIANNULATA- NO DATA PLICAPOLLIS INCISA

COMPLEXIOPOLLIS EX1GUA- SANTALAC1TES MINOR

Figure 20. Chart showing known stratigraphic ranges of pollen taxa in sample R4581 I, Black Creek Group, from 517.0 ft in the Millers Pond core, Burke County, Ga. The identification of taxa followed by an asterisk was checked by R.A. Christopher from photomicrographs provided by the senior author; therefore, these taxa are of greater significance than the others. Full names of taxa are in figure 17 and table 4. Trudopollis sp. cf. T. meekeri is not shown because the stratigraphic range of the species in the eastern United States is unknown. PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C29

SUMMARY len assemblage probably assignable to mid-Campanian Zone CA-4 and has marginal marine or very nearshore Fifty-two Upper Cretaceous samples were examined dinoflagellates. Above this sample in the Millhaven core is a for palynomorphs from four cores (Millhaven, Girard, thick sequence of marine Black Creek sediments that con Thompson Oak, and Millers Pond) in Screven and Burke tains late Campanian calcareous nannofossils of Zone CC Counties, Ga. (table 1). Seventeen of the samples from the 22 in subunit 2 (Bukry, this volume, chap. D) and abundant Millhaven, Girard, and Millers Pond cores contained bio- late Campanian marine dinoflagellates. Two pollen assem stratigraphically useful angiosperm pollen assemblages. blages from subunit 2 and one from subunit 3 indicate Two pollen-bearing samples from the Cape Fear For poorly defined mid-Campanian to Maastrichtian ages. The mation were analyzed, both of them from the Millers Pond lowest part of subunit 3 of the Black Creek Group in the core. They are Coniacian or early Santonian, most probably Millhaven core has the same diverse late Campanian Coniacian, in age. dinoflagellate assemblage as in subunit 2 of the core. How The age of strata mapped as Middendorf Formation ever, the uppermost part of subunit 3 has a less diverse varies from place to place in the Carolinas (Christopher and dinoflagellate assemblage, which indicates minor marine others, 1997). For example, Gohn (1988, 1992), Clarke and influence. others (1994, 1996), and Leeth and others (1996) showed One sample from the Black Creek of the Girard core this formation as being confined to the Santonian, whereas and two samples from the Black Creek of the Millers Pond Lucas-Clark (1992, p. 81) considered the Middendorf to be core contained pollen grains. The Girard assemblage sug "probably Santonian to Campanian in age." Christopher and gests a middle to late Campanian age; one Millers Pond others (1997) stated that at least some strata assigned to the assemblage gave only a poorly defined age, but the other Middendorf in the area of the Savannah River Site are the assemblage seems to be mid-Campanian in age. In the same age as the lowermost part of the Black Creek Group Girard core, dinoflagellate presence and absence data indi (which, according to the present paper, is probably at least cate nonmarine conditions for subunit 1 and the lowermost in part mid-Campanian). part of subunit 2. The data indicate marine conditions for Three samples that contained angiosperm pollen were the remainder of subunit 2 and nonmarine conditions during obtained from the Middendorf Formation in the present deposition of subunit 3 of the Black Creek Group. The study. A sample from the Millhaven core (subunit 2) dinoflagellate taxa in subunit 2 indicate a late Campanian appears to be from Zone V of Coniacian and Santonian age. age. Two samples from the Girard core, from subunits 1 and 2, each contain a seemingly heterogeneous set of taxa whose Two samples of the Black Creek Group from the known occurrences are Coniacian to Santonian, Campanian, Thompson Oak core were examined for dinoflagellates. or Maastrichtian. The peculiar nature of these two assem One sample contained sparse marine dinoflagellates indicat blages seems due to some combination of reworking, drill ing a late Campanian age, and the other lacked dinoflagel ing mud contamination from uphole, species misidentifi- lates. cation, and different species ranges in Georgia than in the Five pollen-bearing samples were analyzed from the Middle Atlantic States. However, at least the pollen flora of Steel Creek Formation, all from the Millhaven core. All of the sample from subunit 2 suggests a latest Santonian(?) or these assemblages appear to be Maastrichtian in age. Two earliest Campanian age. samples from the Steel Creek have dinoflagellates which, if One sample from subunit 2 of the Middendorf Forma indigenous and not representing contamination from tion in the Millhaven core contained marginal marine or uphole, indicate at least a marginally marine paleoenviron- very nearshore marine dinoflagellates. Yet, five samples ment. The Campanian-Maastrichtian boundary in the Mill- examined from the Middendorf of the Girard core con haven core can be shown apparently to coincide with the tained pollen but lacked dinoflagellates and thus are proba contact between the Black Creek Group and the Steel Creek bly nonmarine. Formation by using a combination of pollen and dinoflagel Seven pollen-bearing samples were examined in detail late occurrence data. from the Black Creek Group, from the Millhaven, Girard, and Millers Pond cores. One sample from near the base of All Cretaceous samples from the Millers Pond core the Black Creek (subunit 1) in the Millhaven core has a pol lacked dinoflagellates. C30 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

REFERENCES CITED Clarke, J.S., 1993, Conceptual models of possible stream-aquifer relations in the vicinity of the Savannah River Site, Georgia Aadland, R.K., 1992, Hydrogeologic characterization of the Creta and South Carolina [abs.]: Geological Society of America ceous-Tertiary coastal plain sequence at Savannah River Site, Abstracts with Programs, v. 25, no. 4, p. 8. South Carolina, in Zullo, V.A., Harris, W.B., and Price, Van, Clarke, J.S., Falls, W.F., Edwards, L.E., [Bukry, David,] Frederik- eds., Savannah River region; transition between the Gulf and sen, N.O., Bybell, L.M., Gibson, T.G., Gohn, G.S., and Flem Atlantic Coastal Plains: Proceedings of the Second Bald Head ing, Parley, 1996, Hydrogeologic data and aquifer Island Conference on Coastal Plains Geology, Hilton Head interconnection in a multi-aquifer system in coastal plain sed Island, November 6-11, 1990, p. 62-67. iments near Millhaven, Screven County, Georgia, 1991-95: Aurisano, R.W., 1989, Upper Cretaceous dinoflagellate biostratig- Georgia Geologic Survey Information Circular 99, 43 p., 1 pi. raphy of the subsurface Atlantic Coastal Plain of New Jersey in pocket. and Delaware, U.S.A.: Palynology, v. 13, p. 143-179. Clarke, J.S., Falls, W.F, Edwards, L.E., Frederiksen, N.O., Bybell, Burnett, J.A., 1996, Nannofossils and Upper Cretaceous (sub-) L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, stage boundaries—State of the art: Journal of Nannoplankton hydrologic and water-quality data for a multi-aquifer system Research, v. 18, no. 1, p. 23-32. in coastal plain sediments near Millers Pond, Burke County, Christopher, R.A., 1977a, Selected Normapolles pollen genera and Georgia, 1992-93: Georgia Geologic Survey Information Cir the age of the Raritan and Magothy Formations (Upper Creta cular 96, 34 p., 1 pi. in pocket. ceous) of northern New Jersey, in Owens, J.P., Sohl, N.F., and Clarke, J.S., and West, C.T., 1994, Development of water-table and Minard, J.P., eds., A field guide to Cretaceous and lower Ter potentiometric-surface maps for coastal plain aquifers in the tiary beds of the Raritan and Salisbury embayments, New Jer vicinity of the Savannah River Site, South Carolina and Geor sey, Delaware, and Maryland: Guidebook prepared for the gia [abs.]: Geological Society of America Abstracts with Pro annual AAPG/SEPM convention, Washington, D.C., 1977, p. grams, v. 26, no. 4, p. 8. 58-69. Doyle, J.A., 1969, Cretaceous angiosperm pollen of the Atlantic ————1977b, The stratigraphic distribution of Normapolles and Coastal Plain and its evolutionary significance: Journal of the triporate pollen in Zones IV, V, and VII of the Raritan and Arnold Arboretum, v. 50, p. 1-35. Magothy Formations (Upper Cretaceous) of New Jersey Doyle, J.A., and Robbins, E.I., 1977, Angiosperm pollen zonation [abs.]: American Association of Stratigraphic Palynologists, of the continental Cretaceous of the Atlantic Coastal Plain 10th Annual Meeting, Abstracts with Program, p. 7-8. and its application to deep wells in the Salisbury Embayment: Reprinted 1979 in Palynology, v. 3, p. 281. Palynology, v. 1, p. 43-78. ————1978, Quantitative palynologic correlation of three Campa- Edwards, L.E., 1992, Dinocysts from the lower Tertiary units in the nian and Maestrichtian sections (Upper Cretaceous) from the Savannah River area, South Carolina and Georgia, in Zullo, Atlantic Coastal Plain: Palynology, v. 2, p. 1-27. V.A., Harris, W.B., and Price, Van, eds., Savannah River ————1979, Normapolles and triporate pollen assemblages from region; transition between the Gulf and Atlantic Coastal the Raritan and Magothy Formations (Upper Cretaceous) of Plains: Proceedings of the Second Bald Head Island Confer New Jersey: Palynology, v. 3, p. 73-121, pis. 1-9. ence on Coastal Plains Geology, Hilton Head Island, Novem ————1980, Cretaceous pollen, in Minard, J.P, Geology of the ber 6-11, 1990, p. 97-99. Round Bay quadrangle, Anne Arundel County, Maryland: Edwards, L.E., and Clarke, J.S., 1992, Biostratigraphic investiga U.S. Geological Survey Professional Paper 1109, p. 20-28. tions help evaluation of the ground-water-flow system near ————1982a, Holkopollenites pollen "lineage" from the Upper the Savannah River Site, Georgia and South Carolina [abs.], Cretaceous Series of the Atlantic and Eastern Gulf Coastal in Proceedings, Fifth North American Paleontological Con Plain Province [abs.]: Palynology, v. 6, p. 275-276. vention, Chicago, 111., June 28-July 1, 1992: Paleontological ————1982b, Palynostratigraphy of the basal Cretaceous units of Society Special Publication 6, p. 90. the eastern Gulf and southern Atlantic Coastal Plains, in Edwards, L.E., and Frederiksen, N.O., 1992, Paleogene palyno- Arden, D.D., Beck, B.F., and Morrow, Eleanore, eds.. Pro morph correlations in eastern Georgia [abs.]: Geological ceedings; second symposium on the geology of the southeast Society of America Abstracts with Programs, v. 24, no. 2, p. ern coastal plain: Georgia Geologic Survey Information 14. Circular 53, p. 10-23, pis. 1-3. Edwards, L.E., Frederiksen, N.O., Bybell, L.M., Gohn, G.S., -1982c, The occurrence of the Complexiopollis-Atlantopol- Self-Trail, J.M., Gibson, T.G., Bukry, David, and Fleming, lis Zone (palynomorphs) in the Eagle Ford Group (Upper R.F., 1997, Mysteries solved in the stratigraphy of the updip Cretaceous) of Texas: Journal of Paleontology, v. 56, no. 2, p. coastal plain of Georgia [abs.]: Fifth Annual Clemson Univer 525-541, 1 pi. sity Hydrogeology Symposium, Abstracts, no pagination. Christopher, R.A., Owens, J.P., and Sohl, N.F., 1979, Late Creta Falls, W.F., Baum, J.S., and Prowell, D.C., 1997, Physical stratig ceous palynomorphs from the Cape Fear Formation of North raphy and hydrostratigraphy of Upper Cretaceous and Pale- Carolina: Southeastern Geology, v. 20, no. 3, p. 145-159. ocene sediments, Burke and Screven Counties, Georgia: Christopher, R.A., Prowell, D.C., and Gohn, G.S., 1997, Questions Southeastern Geology, v. 36, p. 153-176. regarding the stratigraphic relationship between the Cape Falls, W.F, Prowell, D.C., Edwards, L.E., Frederiksen, N.O., Gib- Fear and Middendorf Formations [abs.]: Fifth Annual Clem- son, T.G., Bybell, L.M., and Gohn, G.S., 1993, Preliminary son University Hydrogeology Symposium, Abstracts, no pag correlation of geologic units in three coreholes along the ination. Savannah River in Burke and Screven Counties, Georgia PALYNOMORPH BIOSTRATIGRAPHY OF UPPER CRETACEOUS SEDIMENTS FROM FOUR CORES, GEORGIA C31

[abs.]: Geological Society of America Abstracts with Pro Lucas-Clark, Joyce, 1992, Problems in Cretaceous palynostratigra- grams, v. 25, no. 4, p. 14. phy (dinoflagellates and pollen) of the Savannah River Site Firth, J.V., 1987, Dinoflagellate biostratigraphy of the Maastricht- area, in Zullo, V.A., Harris, W.B., and Price, Van, eds., Savan ian to Danian interval in the U.S. Geological Survey Albany nah River region; transition between the Gulf and Atlantic core, Georgia, U.S.A.: Palynology, v. 11, p. 199-216. Coastal Plains: Proceedings of the Second Bald Head Island Frederiksen, N.O., 1979, Paleogene sporomorph biostratigraphy, Conference on Coastal Plains Geology, Hilton Head Island, northeastern Virginia: Palynology, v. 3, p. 129-167. November 6-11, 1990, p. 81-82. Frederiksen, N.O., and Christopher, R.A., 1978, Taxonomy and May, F.E., 1980, Dinoflagellate cysts of the Gymnodiniaceae, Peri- biostratigraphy of Late Cretaceous and Paleogene triatriate diniaceae, and Gonyaulacaceae from the Upper Cretaceous pollen from South Carolina: Palynology, v. 2, p. 113-145. Monmouth Group, Atlantic Highlands, New Jersey: Palaeon Gellici, J.A., andLogan, W.R., 1993, Preliminary stratigraphic and tographica, ser. B, v. 172, p. 10-116. hydrostratigraphic correlation of four deep coreholes east of Olsson, R.K., Gibson, T.G., Hansen, H.J., and Owens, J.P., 1988, the Savannah River Site in Allendale, Barnwell and Aiken Geology of the northern Atlantic coastal plain: Long Island to Counties, South Carolina [abs.]: Geological Society of Amer Virginia, in Sheridan, R.E., and Grow, J.A., eds., The Atlantic ica Abstracts with Programs, v. 25, no. 4, p. 17. continental margin; U.S, v. 1-2 of Geology of North America: Gohn, G.S., 1988, Late Mesozoic and early Cenozoic geology of Boulder, Colo., Geological Society of America, p. 87-105. the Atlantic Coastal Plain: North Carolina to Florida, in Perch-Nielsen, Katharina, 1985, Mesozoic calcareous nannofos- Sheridan, R.E., and Grow, J.A., eds., The Atlantic continental sils, in Bolli, H.M., Saunders, J.B., and Perch-Nielsen, Katha margin; U.S., v. 1-2 of Geology of North America: Boulder, rina, eds.. Plankton stratigraphy: New York, Cambridge Colo., Geological Society of America, p. 107-130. University Press, p. 329^126. ————1992, Revised nomenclature, definitions, and correlations Prowell, D.C., Christopher, R.A., Edwards, L.E., Bybell, L.M., and for the Cretaceous formations in USGS-Clubhouse Cross Gill, H.E., 1985 [1986], Geologic section of the updip coastal roads #1, Dorchester County, South Carolina: U.S. Geologi plain from central Georgia to western South Carolina: U.S. cal Survey Professional Paper 1518, 39 p., 1 pi. in pocket. Geological Survey Miscellaneous Field Studies Map MF- Gray, T.C., and Groot, J.J., 1966, Pollen and spores from the 1737, 10-p. text, 1 sheet. marine Upper Cretaceous formations of Delaware and New Prowell, D.C., Edwards, L.E., and Frederiksen, N.O., 1985 [1986], Jersey: Palaeontographica, ser. B, v. 117, p. 114-134. The Ellenton Formation in South Carolina—A revised age Habib, Daniel, and Miller, J.A., 1989, Dinoflagellate species and designation from Cretaceous to Paleocene, //; Stratigraphic organic facies evidence of marine transgression and regres notes, 1984: U.S. Geological Survey Bulletin 1605-A, p. sion in the Atlantic Coastal Plain: Palaeogeography, Palaeo- A63-A69. climatology, Palaeoecology, v. 74, p. 23^-7. Self-Trail, J.M., and Bybell, L.M., 1995, Cretaceous and Paleo Habib, Daniel, Olsson, R.K., Liu, Chengjie, and Moshkovitz, Shi- gene calcareous nannofossil biostratigraphy of New Jersey, in mon, 1996, High-resolution biostratigraphy of sea-level low, Baker, J.E.B., ed., Contributions to the paleontology of New biotic extinction, and chaotic sedimentation at the Creta Jersey: Geological Association of New Jersey Contribution ceous-Tertiary boundary in Alabama, north of the Chicxulub Proceedings, v. 12, p. 102-139. crater, in Ryder, G., Fastovsky, D., and Gartner, S., eds., The Sirkin, L.A., 1974, Palynology and stratigraphy of Cretaceous Cretaceous-Tertiary event and other catastrophes in Earth his strata in Long Island, N.Y, and Block Island, Rhode Island: tory: Geological Society of America Special Paper 307, p. U.S. Geological Survey Journal of Research, v. 2, p. 431^140. 243-252. Sohl, N.F., Martmez R., Eduardo, Salmeron-Urena, Pedro, and Harris, M.K., Aadland, R.K., and Westbrook, T.M., 1992, Litho- Soto-Jaramillo, Fidel, 1991, Upper Cretaceous, in Salvador, logical and hydrological characteristics of the Tertiary Amos, ed., The Gulf of Mexico Basin, v. J of Geology of hydrostratigraphic systems of the General Separations Area, North America: Boulder, Colo., Geological Society of Amer Savannah River Site, South Carolina, in Zullo, V.A., Harris, ica, p. 205-244. W.B., and Price, Van, eds., Savannah River region; transition Srivastava, S.K., 1991, Cenomanian-Coniacian dinocysts from the between the Gulf and Atlantic Coastal Plains: Proceedings of western Gulf Coastal Plain, southern United States: Palaeo- the Second Bald Head Island Conference on Coastal Plains botanist, v. 39, no. 2, p. 155-235. Geology, Hilton Head Island, November 6-11, 1990, p. 68- ————1993, Dinocyst biostratigraphy of Santonian-Maastrichtian 73. formations of the western Gulf Coastal Plain, southern United Koch, R.C., and Olsson, R.K., 1977, Dinoflagellate and planktonic States: Palaeobotanist, v. 42, no. 3, p. 249-362. foraminiferal biostratigraphy of the uppermost Cretaceous of Stover, L.E., Elsik, W.C., and Fairchild, W.W., 1966, New genera New Jersey: Journal of Paleontology, v. 51, p. 480^191. and species of early Tertiary palynomorphs from Gulf Coast: Leeth, D.C., Falls, W.F., Edwards, L.E., Frederiksen, N.O., and Kansas University Paleontological Contributions, Paper 5, 10 Fleming, R.F., 1996, Geologic, hydrologic, and water-chem P- istry data for a multi-aquifer system in coastal plain sediments Strom, R.N., Kaback, D.S., and Schramke, J.A., 1992, Groundwa- near Girard, Burke County, Georgia, 1992-95: Georgia Geo ter geochemistry and flow path modeling, Savannah River logic Survey Information Circular 100, 26 p., 1 pi. Site, S.C. [abs.]: Geological Society of America Abstracts Litwin, R.J., Sohl, N.F., Owens, J.P, and Sugarman, P.J., 1993, with Programs, v. 24, no. 2, p. 69. Palynological analysis of a newly recognized Upper Creta Sugarman, P.J., Miller, K.G., Bukry, David, and Feigenson, M.D., ceous marine unit at Cheesequake, New Jersey: Palynology, v. 1995, Uppermost Campanian-Maestrichtian strontium isoto- 17, p. 123-135, pis. 1-3. pic, biostratigraphic, and sequence stratigraphic framework of C32 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

the New Jersey Coastal Plain: Geological Society of America Whitney, B.L., 1979, A population study ofAlterbia acutula (Wil Bulletin, v. 107, p. 19-37. son) Lentin & Williams from the Maestrichtian (Upper Creta Thomson, P.W., and Pflug, H.D., 1953, Pollen und Sporen des mit- ceous) of Maryland: Palynology, v. 3, p. 123-128. teleuropaischen Tertiars: Palaeontographica, ser. B, v. 94, 138 P- Wolfe, J.A., 1976, Stratigraphic distribution of some pollen types Tschudy, R.H., 1970, Two new pollen genera (Late Cretaceous and from the Campanian and lower Maestrichtian rocks (Upper Paleocene) with possible affinity to the Illiciaceae: U.S. Geo Cretaceous) of the Middle Atlantic States: U.S. Geological logical Survey Professional Paper 643-F, p. F1-F13. Survey Professional Paper 977, 18 p., 4 pis. ————1973, Complexiopollis pollen lineage in Mississippi embayment rocks: U.S. Geological Survey Professional Paper Zaitzeff, J.B., and Cross, A.T., 1971, The use of dinoflagellates 743-C, 15 p. and acritarchs for zonation and correlation of the Navarro ————1975, Normapolles pollen from the Mississippi embay Group (Maastrichtian) of Texas: Geological Society of Amer ment: U.S. Geological Survey Professional Paper 865, 42 p. ica Special Paper 127, p. 341-377. PLATES 1-7 PLATE 1

[All specimens are from Screven and Burke Counties, Georgia]

Figure 1. Rugubivesiculites sp., Middendorf Formation, subunit 1, Girard core (1,138.0- 1,139.0 ft), Burke County. 2. Triatriopollenites sp.. Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. 3. Momipites microfoveolatus (Stanley) Nichols, Steel Creek Formation, Millhaven core (824.1-824.4 ft), Screven County. 4. Triatriopollenites sp., Black Creek Group, Millers Pond core (517.0 ft), Burke County. 5. Momipites tenuipolus group of Frederiksen and Christopher (1978), Steel Creek Formation, Millhaven core (824.1-824.4 ft), Screven County. This species group is characterized by having a ring of thin exine about one pole. In the present specimen, the ring is triangular in shape, and only two sides of the ring are distinct. 6, 7. Momipites n. sp. 1, Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. 8. Aff. NP-2 of Wolfe (1976), Steel Creek Formation, Millhaven core (830.3-830.5 ft), Screven County. In this specimen, the exine is slightly thicker than in NP-2 but thinner than in NP-1. 9. NP-2 of Wolfe (1976), Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. 10-12. Momipites n. sp. 1, Steel Creek Formation, Millhaven core (824.1-824.4 ft, 829.5- 829.8 ft, and 824.1-824.4 ft, respectively), Screven County. 13. N20-12 of R.A. Christopher (unpublished), Black Creek Group, subunit 2, Girard core (738.3-738.6 ft). Burke County. The pores protrude considerably less than in NO-3 of Wolfe (1976) (R.A. Christopher, written commun., 1996). 14. Casuarinidites sp. A of Frederiksen and Christopher (1978), Black Creek Group, subunit 2, Millhaven core (941.7-941.9 ft), Screven County. Many specimens assigned to this species in the present material have one or two pores offset onto one face of the grain, and in this respect they are very similar to the Tertiary genus Subtriporopollenites. 15, 16. PR-7 of Wolfe (1976), Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. 17. Casuarinidites sp. A of Frederiksen and Christopher (1978), Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. 18. PR-1 of Wolfe (1976), Black Creek Group, subunit 1, Millhaven core (1,124.3- 1,124.7 ft), Screven County. 19-21. Cf. Triporate type 4 of Christopher (1979), Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C. PLATE 1

14 15 16

19 20 21

j____I 0 20 40 Jim

POLLEN PLATE 2

[All specimens are from Screven and Burke Counties, Georgia]

Figure 1. PR-1 of Wolfe (1976), Black Creek Group, subunit 2, Millhaven core (941.7-941.9 ft), Screven County. 2. Interporopollenites turgidus Tschudy, Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. 3, 4. Trisectoris costatus Tschudy, Black Creek Group, subunit 2, Millhaven core (941.7-941.9 ft), Screven County. 5. Tricolpites sp., Black Creek Group, Millers Pond core (517.0 ft), Burke County. 6, 7. Tricolpites sp., Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. 8. Aff. Plicapollis sp. A of Christopher (1979), Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. 9. Plicapollis sp. K of Christopher (1979), Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. 10. Complexiopollis funiculus Tschudy, Cape Fear Formation, Millers Pond core (827.0-832.0 ft), Burke County. 11. Complexiopollis abditus Tschudy, Middendorf Formation, subunit 2, Girard core (1,012.0-1,012.3 ft), Burke County. 12. Complexiopollis sp., Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. 13. New genus A of Tschudy (1975), Cape Fear Formation, Millers Pond core (797.0- 802.0 ft), Burke County. 14. Probably Praecursipollis plebius Tschudy, Black Creek Group, subunit 1, Millhaven core (1,124.7-1,124.3 ft), Screven County. 15. Praecursipollis plebius Tschudy, Cape Fear Formation, Pond core (827.0-832.0 ft), Burke County. Two sides of the grain have been folded inward. 16. Cf. ND-2 of Wolfe (1976), Black Creek Group, subunit 2, Millhaven core (941.7- 941.9 ft), Screven County. Plicae are present but very weak; an interloculum is lacking. 17-19. Complexiopollis! sp., Cape Fear Formation, Millers Pond core (827.0-832.0 ft), Burke County. 20. New genus D, sp. H of Christopher (1979), Black Creek Group, subunit 1, Millhaven core (1,124.3-1,124.7 ft), Screven County. 21. New genus D, sp. B of Christopher (1979), Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 2

12 13

0 20 40|im 17 18 19

POLLEN PLATE 3

[All specimens are from Screven and Burke Counties, Georgia]

Figure 1. New genus D, sp. J of Christopher (1979), Middendorf Formation, subunit 1, Girard core (1,138.0-1,139.0 ft), Burke County. 2. New genus D, sp. L of Christopher (1979), Black Creek Group, subunit 1, Millhaven core (1,124.3-1,124.7 ft), Screven County. 3-5. N20-2 of R.A. Christopher (unpublished), Black Creek Group, subunit 1, Millhaven core (1,124.3-1,124.7 ft), Screven County. 6, 7. IPorocolpopollenites sp. A of Christopher and others (1979), Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. 8. Porocolpopollenites n. sp. 1, Cape Fear Formation, Millers Pond core (797.0- 802.0 ft), Burke County. 9. Trudopollis sp. cf. T. meekeri Newman, Black Creek Group, Millers Pond core (517.0ft), Burke County. 10, 11. Rhombipollis sp., Black Creek Group, Millers Pond core (517.0 ft), Burke County. 12. CP3F-1 of Wolfe (1976), Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. This specimen is similar both to CP3F-1 and to Brevicolporites sp. A of Christopher (1978). 13. CP3F-1 of Wolfe (1976), Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. 14, 15. Brevicolporites sp., Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County. 16. Lanagiopollis cribellatus (Srivastava) Frederiksen, Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 3

10 11 12 13

14 J_____L 0 20 40 Jim

POLLEN PLATE 4

[All specimens are from Screven and Burke Counties, Georgia]

Figures 1, 2. Brevicolporites sp. A of Christopher (1980), Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. Brevicolporites sp. A of Christopher (1980) is not exactly the same as Brevicolporites sp. A of Christopher (1978) nor as CP3F-1 of Wolfe (1976). 3. CP3D-3 of Wolfe (1976), Black Creek Group, Millers Pond core (517.0 ft), Burke County. 4, 5. Brevicolporites sp. A of Christopher (1978), Middendorf Formation, subunit 2, Girard core (1,012.0-1,012.3 ft), Burke County. These specimens seem to differ fromCP3F-l of Wolfe (1976). 6. Tricolporites sp., Cape Fear Formation, Millers Pond core (797.0-802.0 ft), Burke County. 7. Aff. C3C-1 of Wolfe (1976), Steel Creek Formation, Millhaven core (769.0-769.3 ft), Screven County. 8. CP3G-1 of Wolfe (1976), Middendorf Formation, subunit 1, Girard core (1,138.0- 1,139.0ft), Burke County. 9. Tricolporites sp., Middendorf Formation, subunit 2, Girard core (1,012.0-1,012.3 ft), Burke County. 10, 11. Nyssapollenites sp., Middendorf Formation, subunit 2, Girard core (1,012.0- 1,012.3 ft), Burke County. 12, 13. CP3E-1 of Wolfe (1976), Middendorf Formation, subunit 1, Girard core (1,138.0- 1,139.0ft), Burke County. 14, 15. Holkolpollenites sp., Steel Creek Formation, Millhaven core (829.5-829.8 ft), Screven County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 4

10 11

14 15

12 13 j____I____1 0 20 40 Jim

POLLEN PLATE 5

[All specimens are from Screven and Burke Counties, Georgia]

Figures 1-3. CP3D-3 of Wolfe (1976), Black Creek Group, subunit 2. 1, Girard core (738.3- 738.6 ft), Burke County; 2, 3, Millhaven core (1,029.5 ft), Screven County. 4-9. CP3E-1 of Wolfe (1976). 4, 5, Black Creek Group, subunit 2, Girard core (738.3- 738.6 ft), Burke County; 6, 7, Middendorf Formation, subunit 1, Girard core (1,138.0-1,139.0 ft), Burke County; 8, 9, Steel Creek Formation, Millhaven core (824.1-824.4 ft), Screven County. 10, 11. Cf. MPH-1 of Wolfe (1976), Steel Creek Formation, Millhaven core (830.3-830.5 ft), Screven County. MPH-1 of Wolfe = Baculostephanocolpites sp. A of Christopher (1980) has distinct columellae, whereas the present specimen has barely perceptible columellae. 12, 13. Tetracolporate sp., Steel Creek Formation, Millhaven core (830.3-830.5 ft), Screven County. 14. Holkopollenites sp., Middendorf Formation, subunit 2, Girard core (1,012.0- 1,012.3 ft), Burke County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 5

10 12

J___I 13 0 20 40|iim

POLLEN PLATE 6

[Upper scale bar is for specimens at x 400; lower scale bar is for specimens at x 600. All specimens are from the Black Creek Group in Screven and Burke Counties, Georgia]

Figure 1. Alisogymnium euclaense (Cookson & Eisenack) Lentin & Vozzhennikova, Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; ?ventral view at mid-focus (x 600). 2. Dinogymnium acuminatum Evitt et al., Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; orientation unknown at high focus (x 600). 3. Alterbidinium acutulum (Wilson) Lentin & Williams, Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; dorsal view of dorsal surface (x 400). 4. lAndalusiella spicata (May) Lentin & Williams, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; ventral view of dorsal surface (x400). This form is an end member in a plexus that includes A. spicata (May) Lentin & Williams. Considerable variation exists in the surface texture, relative archeopyle size, and horn lengths. 5. Andalusiella polymorpha (Malloy) Lentin & Williams, Black Creek Group, subunit 3, Millhaven core (913.8-914.2 ft), Screven County; left lateral view at mid-focus (x 400). 6. Andalusiella spicata (May) Lentin & Williams, Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; ventral view of dorsal surface (x 400). 7. Cerodinium pannuceum (Stanley) Lentin & Williams, Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; dorsal view of dorsal surface (x 400). 8. Cerodinium striatum (Drugg) Lentin & Williams, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; ventral view at mid-focus (x 400). 9. Cordosphaeridiumfibrospinosum Davey & Williams, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft) Screven County; left lateral view at mid-focus (x 400). 10. Cribroperidinium sp., Black Creek Group, subunit 3, Millhaven core (913.8-914.2), Screven County; ventral view at mid-focus (x 400). 11. Diphyes recurvatum May, Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; orientation unknown at mid-focus (x 600). 12. Exochosphaeridium sp., Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; dorsal view of dorsal surface (x 400). 13. Fromea sp., Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; orientation unknown at low focus (x 400). 14. Fromea sp., Black Creek Group, subunit 3, Millhaven core (913.8-914.2 ft), Screven County; orientation unknown at mid-focus (x 400). 15. Membranosphaera maastrictica Samoilovitch, Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; ventral view at mid-focus (x 600). 16. Operculodinium sp., Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; left lateral view at mid-focus (x 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 6

0 20 40 |im 15 16

DINOFLAGELLATES AND ACRITARCHS PLATE 7

[Upper scale bar is for specimens at x 400; lower scale bar is for specimens at x 600. All specimens are from Screven and Burke Counties, Georgia]

Figure 1. Odontochitina costata Albert!, Black Creek Group, subunit 2, Girard core (868.5- 868.7 ft), Burke County; ventral view at mid-focus (x 400). 2. Palaeohystrichophora infusorioides Deflandre, Middendorf Formation, subunit 2, Millhaven core (1,212.0 ft), Screven County; dorsal view of dorsal surface (x400). 3. Palaeohystrichophora infusorioides Deflandre, Middendorf Formation, subunit 2, Millhaven core (1,212.0 ft), Screven County; orientation unknown at mid-focus (x400). 4. Palaeoperidinium sp., Middendorf Formation, subunit 2, Millhaven core (1,212.0 ft), Screven County; ventral view at mid-focus (x 400). 5. Tanyosphaeridium xanthiopyxides (Wetzel) Stover & Evitt, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; orientation unknown at mid-focus (x 600). 6. Spiniferites sp., Black Creek Group, subunit 2, Girard core (834.6-834.8 ft), Burke County; orientation unknown at high focus (x 400). 7. Spongodinium delitiense (Ehrenberg) Deflandre, Steel Creek Formation, Millhaven core (830.3-830.5 ft), Screven County; isolated operculum (x 400). 8, 9. Tricodinium castanea (Deflandre) Clark & Verdier, Black Creek Group, subunit 2, Girard core (834.6-834.8 ft), Burke County; ventral views of ventral surface (8) and dorsal surface (9) (both x 400). 10. Small peridiniacean form, Black Creek Group, subunit 1, Millhaven core (1,124.3- 1,124.7 ft), Screven County; dorsal view of dorsal surface (x400). 11. Small peridiniacean form, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; dorsal view of dorsal surface (x 400). 12. Small peridiniacean form, Black Creek Group, subunit 2, Girard core (868.5-868.7 ft), Burke County; dorsal view of dorsal surface (x 400). 13. Small peridiniacean form, Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; dorsal view of dorsal surface (x 400). 14. Hystrichosphaeridium tubiferum (Ehrenberg) Deflandre, Black Creek Group, subunit 2, Girard core (738.3-738.6 ft), Burke County; orientation unknown at mid-focus (x 400) [included in tables and figures under "miscellaneous chorale forms"]. 15. Miscellaneous areoligeracean form, Black Creek Group, subunit 1, Millhaven core (1,124.3-1,124.7 ft), Screven County; dorsal view at mid-focus (x 400). 16. Miscellaneous areoligeracean form, Black Creek Group, subunit 1, Millhaven core (1,124.3-1,124.7 ft), Screven County; ventral view at mid-focus (x 400). 17. Miscellaneous areoligeracean form, Black Creek Group, subunit 3, Millhaven core (913.8-914.2 ft), Screven County; dorsal view of dorsal surface? (x 400). 18. Lejeunecysta sp., Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; dorsal view of dorsal surface (x 400). 19. Xenascus ceratioides (Deflandre) Lentin & Williams, Black Creek Group, Thompson Oak core (505.0 ft), Burke County; dorsal view at mid-focus (x 400). 20. Small peridiniacean form, Black Creek Group, subunit 2, Millhaven core (1,029.5 ft), Screven County; ventral view of ventral surface (x 600). 21. Miscellaneous areoligeracean form, Black Creek Group, subunit 2, Girard core (834.6-834.8 ft), Burke County; dorsal view? at mid-focus (x 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-C, PLATE 7

20 40 |im

DINOFLAGELLATES

U.S. Department of the Interior U.S. Geological Survey

Late Campanian (Zone CC 22) Coccoliths from the Millhaven Core, Screven County, Georgia By David Bukry

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-D

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract ...... Dl Introduction ...... 1 Acknowledgments ...... 1 Material and Methods ...... 1 Georgia Coccoliths ...... 1 New Jersey Coccoliths ...... 2 Comparison of Campanian Coccolith Floras in the Atlantic Coastal Plain and California ...... 2 Conclusions ...... 4 References Cited ...... 4

FIGURE

1. Index map showing the Savannah River Site and the location of the Millhaven test hole in Screven County, Georgia...... ^ D2

TABLES

1. U.S. Geological Survey Millhaven core coccolith checklist...... D3 2. Coccolith taxa considered in this report...... 4

III

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Late Campanian (Zone CC 22) Coccoliths from the Millhaven Core, Screven County, Georgia

By David Bukry

ABSTRACT ACKNOWLEDGMENTS

I thank Gregory S. Gohn and Lucy E. Edwards (U.S. Coccolith floras from the Millhaven core in Screven Geological Survey) for providing samples and supporting County, Georgia, from depths of 1,077 to 968 feet, belong to information about the Georgia research. I thank Kevin Pur- late Campanian Zone CC 22. The co-occurrence of zonal cell (USGS) for doing special sample preparations for gen guide species Quadrum trifidum (Stradner) Prins & eral matrix and coherent rock chips for each sample and for Perch-Nielsen and Reinhardtites anthophorus (Deflandre) processing the text. Special appreciation goes to Peter J. Perch-Nielsen permits direct correlation with the paleomag- Sugarman (New Jersey Geological Survey) and Norman F. netically dated Point Loma Formation in California. Q. trifi Sohl and James Owens (U.S. Geological Survey, both dum (Stradner) Prins & Perch-Nielsen, a warm-water taxon, deceased) for providing New Jersey core and outcrop sam is consistently present in the Georgia and California sec ples as an extension of our joint studies from 1989 to 1994. tions but is missing from the late Campanian floras that Michael P. Kennedy (California Division of Mines and occur in the northern Atlantic Coastal Plain in New Jersey. Geology), George W. Moore (U.S. Geological Survey), Annika Sanfilippo (University of California, San Diego/ Scripps Institution of Oceanography), and Thomas A. Demere (San Diego Natural History Museum) helped me to INTRODUCTION collect the California core and outcrop samples.

Four core samples were examined for coccolith con tent from the U.S. Geological Survey Millhaven test hole MATERIAL AND METHODS (lat 32°53'25" N., long 81°35'43" W.), which is located in Screven County, Ga. (fig. 1). These samples were studied to Samples from the Millhaven core and outcrop samples supplement biostratigraphic dating of the Cretaceous marine from New Jersey and California were prepared for sediments in the core interval from the 1,099 to 927 ft. This light-microscope examination (magnifications x 600 and Cretaceous interval is considered to be part of the Black x 1560) using the technique described in Bukry and Creek Group, which ranges in age from middle to late Cam Kennedy (1969). Zonal assignments are based on Perch-Nielsen (1985, p. 342), and stage assignments are panian in the Millhaven core (Falls and Prowell, this vol based on Sissingh (1977) and Burnett and others (1992). ume, chap. A; Edwards and others, this volume, chap. B). Samples studied for this report represent all but the lowest 20 ft of the Black Creek Group subunit 2 of Falls and Prow- GEORGIA COCCOLITHS ell (this volume, chap. A). Comparative coccolith samples from New Jersey and California Cretaceous strata also were Coccoliths from the Millhaven core (table 1) are used in this study. The Californian floras have been pub slightly etched and common to abundant. Floras have mod lished previously by Bukry and Kennedy (1969) and Bukry erate to high species diversity (number of species («)=15 to (1993, 1994). Coccoliths identified from the Millhaven core 30). The most common species are dissolution-resistant are listed in table 1, and all taxa considered in this report are Micula decussata Vekshina and Reinhardtites anthophorus listed in table 2. (Deflandre) Perch-Nielsen. Other stratigraphic guide spe- Dl D2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 30' 81 ° 30' 1995). This late Campanian correlation is based on the iden tifications of key coccolith species Broinsonia parca (Strad ner) Bukry, Calculites obscurus (Deflandre) Prins & Sissingh, Reinhardtites anthophorus (Deflandre) Perch- Nielsen, R. levis Prins & Sissingh, and Tranolithus phacelosus Stover. The warm-water biostratigraphic guide species 33° 30' Quadrum trifidum (Stradner) Prins & Perch-Nielsen and Quadrum sissinghii Perch-Nielsen are missing from New Jersey floras (Bukry, 1990). The absence of Quadrum trifidum (Stradner) Prins & Perch-Nielsen in New Jersey floras may be attributed to its general global distribution pattern and local ecological con 33° ditions. Roth (1978) described Q. trifidum (Stradner) Prins & Perch-Nielsen as a temperature-sensitive, warm-water species. Thierstein (1981, fig. 21) demonstrated maximum abundances within approximately 30 degrees latitude of the paleoequator for Q. trifidum (Stradner) Prins & Perch- Nielsen. Doeven (1983) used this information to suggest that in Canadian Atlantic well sites, the top range of Q. trifi 32° 30' dum (Stradner) Prins & Perch-Nielsen might be depressed as a result of decreased paleotemperatures. Further, he reported only rare abundances at Canadian sites. Similarly, Millhaven • Test hole site and informal name of site Burnett and others (1992) reported only sporadic occur rences of Q. trifidum (Stradner) Prins & Perch-Nielsen in sections from Germany and Poland. This occurrence pattern Figure 1. Index map showing the Savannah River Site and the contrasts with the rare to common but consistent occur location of the Millhaven test hole in Screven County, Georgia. rences in California (Bukry, 1993, 1994) and the consistent presence in the Georgia core samples studied here. cies such as Broinsonia parca (Stradner) Bukry, Calculites Similar consistent occurrences were cited in Israel obscurus (Deflandre) Prins & Sissingh, Ceratolithoides (Moshkovitz, 1984), supporting warm-water affinities for aculeus (Stradner) Prins & Sissingh, Quadrum trifidum Quadrum trifidum (Stradner) Prins & Perch-Nielsen. The (Stradner) Prins & Perch-Nielsen, and R. levis Prins & Siss late Campanian Mount Laurel Formation floras from New ingh are present in smaller numbers. All four of the closely Jersey lack Q. trifidum (Stradner) Prins & Perch-Nielsen but spaced floras (1,077, 1,021.5, 971, and 968 ft) contain both were assigned to Zone CC 22 or Subzone CC 22b based on Q. trifidum (Stradner) Prins & Perch-Nielsen and R. antho- the co-occurrence of other taxa, principally Reinhardtites phorus (Deflandre) Perch-Nielsen, which together define anthophorus (Deflandre) Perch-Nielsen and R. levis Prins & late Campanian Zone CC 22. Reinhardtites levis Prins & Sissingh. The highest occurrence of R. anthophorus Sissingh, which has been designated a guide species for (Deflandre) Perch-Nielsen defines the top of Zone CC 22 in upper Subzone CC 22b, occurs only rarely in the bottom the late Campanian. In cooler water floras, the co-occur and top samples. It is missing in the most diverse (n=30) rence of R. levis Prins & Sissingh with R. anthophorus sample at 1,021.5 ft. In the sample taken at 971 ft, only two (Deflandre) Perch-Nielsen is considered a useful indicator specimens of Reinhardtites sp. cf. R. levis Prins & Sissingh for Subzone CC 22b (Perch-Nielsen, 1985, p. 347). were identified. Evidence from floras in California and Israel suggests that R. levis Prins & Sissingh has a longer range in CC 21 and CC 22 at middle latitudes (Bukry, 1994; COMPARISON OF CAMPANIAN Eshet and Moshkovitz, 1995). The best coccolith assign COCCOLITH FLORAS IN THE ATLANTIC ment for all four Georgia floras from the Millhaven core is COASTAL PLAIN AND CALIFORNIA late Campanian Zone CC 22. The Point Loma Formation in San Diego County, Calif, contains the same key coccolith species in late Cam NEW JERSEY COCCOLITHS panian Zone CC 22 that occur in the Georgia floras. The consistent occurrence of Quadrum trifidum (Stradner) Prins Outcrop and core samples from the Upper Cretaceous & Perch-Nielsen in the Georgia floras matches the pattern in Mount Laurel Formation in New Jersey contain coccolith Point Loma core hole DH-1 where it occurs in 30 of 31 coc- floras assigned to Subzone CC 22b (Sugarman and others, colith-bearing samples from CC 22 (Bukry, 1993). Both LATE CAMPANIAN (ZONE CC 22) COCCOLITHS FROM THE MILLHAVEN CORE, SCREVEN COUNTY, GEORGIA D3

Table 1. U.S. Geological Survey Millhaven core coccolith checklist.

Sample depth, in feet

Coccolith 1,077 1,021.5 971

Arkhangelskiella cymbiformis —————— X Biscutum sp.————————————— Broinsonia parca parca—————————— X Broinsonia parca constricta -——-——— X Calculates obscurus ——————————— Ceratolithoides aculeus ———————— X Chiastozygus amphipons ——————— Chiastozygus sp. ——————————————— X Coronocyclus sp. ——————————— Cretarhabdus crenulatus ———————— X Cribrosphaera ehrenbergii—————-—— X Eiffellithus eximius —————————— Eiffellithus turriseiffelii———————— X Gartnemgo concavum ————————— Gartnerago costatum ————————— Kamptnerius magnificus———————— X Lithraphidites carniolensis——————— Lucianorhabdus cayeuxii——————— Lucianorhabdus maleformis —————— Microrhabdulus decoratus ——————— Micula concava——————————— Micula decussata———————————— X Parhabdolithus embergeri——————— X Prediscosphaera cretacea ——————— X Prediscosphaera spinosa ————————— Quadrum sissinghii —————————— X Quadrum trifidum —————————— X Reinhardtites anthophorus ——————— X Reinhardtites levis—————————— X Reinhardtites sp. cf. R. levis —————— Rucinolithus sp.———————————— Tranolithus phacelosus ————————— Vagalapilla octoradiata———————— X Watznaueria barnesae ———————— X Watznaueria biporta ——————————— X Zygodiscus bicrescenticus—————-—— x Zygodiscus spiralis——————————— sites are part of a warm-water regime, but the Point Loma netochronostratigraphic Chron 33n (Bannon and others, flora lacks Calculites obscurus (Deflandre) Prins & Siss- 1989, fig. 3) in the late Campanian (Bannon and others, ingh, Kamptnerius magnificus Deflandre, Lucianorhabdus 1989; Bukry, 1994). The key La Jolla coccoliths in the cayeuxii Deflandre, and Tranolithus phacelosus Stover. Chron 33n portion of Subzone CC 22b include Broinsonia These absences reflect deep-water deposition for the Point parca (Stradner) Bukry, Q. trifidum (Stradner) Prins & Loma core strata. In shallower water strata of the Point Perch-Nielsen, Q. sissinghii Perch-Nielsen, Reinhardtites Loma Formation in Carlsbad, Calif., some C. obscurus anthophorus (Deflandre) Perch-Nielsen, and R. levis Prins (Deflandre) Prins & Sissingh and L. cayeuxii Deflandre & Sissingh, which enable direct correlation of late Campa were recorded (Bukry, 1994). nian paleomagnetic Chron 33n with the four Georgia floras At La Jolla, Calif., floras assigned to CC 22b occur in assigned to the Black Creek Group. The disappearance of/?. a 280-ft stratigraphic section that has been assigned to mag- anthophorus (Deflandre) Perch-Nielsen in Europe predates D4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Table 2. Coccolith taxa considered in this report. REFERENCES CITED Arkhangelskiella cymbiformis Vekshina Broinsonia parca (Stradner) Bukry Bannon, J.L., Bottjer, D.J., Lund, S.P, and Saul, L R., 1989, Cam- Broinsonia parca constricta Hattner et al. panian/Maestrichtian stage boundary in southern California: Calculites obscunis (Deflandre) Prins & Sissingh in Sissingh Resolution and implications for large-scale depositional pat Ceratolithoides aculeus (Stradner) Prins & Sissingh in Sissingh terns: Geology, v. 17, p. 80-83. Chiastozygus amphipons (Bramlette & Martini) Gartner Bukry, David, 1990, Remarks on calcareous and siliceous nanno- Cretarhabdus crenulatus Bramlette & Martini plankton biostratigraphy for some Cretaceous and Tertiary Cribrosphaera ehrenbergii Arkhangelsky core samples from southern New Jersey: U.S. Geological Sur Eiffellithus eximius (Stover) Perch-Nielsen vey Open-File Report 90-278, 22 p. Eiffellithus turriseiffelii (Deflandre) Reinhardt ————1993, Cretaceous coccolith correlation for Point Loma For Gartnerago concavum (Gartner) Bukry mation outfall test well, San Diego, California: U.S. Geologi Gartnerago costatum (Gartner) Bukry cal Survey Open-File Report 93-567, 14 p. Kamptnerius magnificus Deflandre ————1994, Coccolith correlation of Late Cretaceous Point Loma Lithraphidites camiolensis Deflandre Formation at La Jolla and Carlsbad, San Diego County, Cali Lucianorhabdus cayeuxii Deflandre fornia: U.S. Geological Survey Open-File Report 94-678, Lucianorhabdus maleformis Reinhardt 23 p. Microrhabdulus decoratus Deflandre Bukry, David, and Kennedy, M.P., 1969, Cretaceous and Eocene Micula concava (Stradner in Martini and Stradner) Verbeek coccoliths at San Diego, California: California Division of Micula decussata Vekshina Mines and Geology Special Report 100, p. 33-43. Parhabdolithus embergeri (Noel) Stradner Prediscosphaera cretacea (Arkhangelsky) Gartner Burnett, J.A., Hancock, J.M., Kennedy, W.J., and Lord, A.R., Prediscosphaera spinosa (Bramlette & Martini) Gartner 1992, Macrofossil, planktonic foraminiferal and nannofossil zonation at the Campanian/Maastrichtian boundary: Newslet Quadrum sissinghii Perch-Nielsen ters on Stratigraphy, v. 27, p. 157-172. Quadrum trifidum (Stradner) Prins & Perch-Nielsen in Manivit Reinhardtites anthophorus (Deflandre) Perch-Nielsen Doeven, PH., 1983, Cretaceous nannofossil stratigraphy and pale- Reinhardtites levis Prins & Sissingh oecology of the Canadian Atlantic margin: Geological Survey Tranolithus phacelosus Stover of Canada Bulletin 356, 69 p. Vagalapilla octoradiata (Gorka) Bukry Eshet, Yoram, and Moshkovitz, Shimon, 1995, New nannofossil Watznaueria bamesae (Black) Perch-Nielsen biostratigraphy for Upper Cretaceous organic-rich carbonates Watznaueria biporta Bukry in Israel: Micropaleontology, v. 41, no. 4, p. 321-341. Zygodiscus bicrescenticus (Stover) Bukry Moshkovitz, Shimon, 1984, Late Cretaceous calcareous nannofos Zygodiscus spiralis Bramlette & Martini sil biostratigraphy of the Mount Scopus Group, Israel: Geo logical Survey of Israel Current Research 1983-84, p. 46-60. the appearance of the cephalopod Belemnella lanceolata Perch-Nielsen, Katharina, 1985, Mesozoic calcareous nannofos- (basal Maastrichtian) (Burnett and others, 1992) and helps sils, in Bolli, H.M., Saunders, J.B., and Perch-Nielsen, Katha to confirm the late Campanian age for the correlated CC 22b rina, eds., Plankton stratigraphy: New York, Cambridge University Press, p. 329-426. coccolith floras on the Atlantic and Pacific coasts. Roth, PH., 1978, Cretaceous nannoplankton biostratigraphy and oceanography of the northwestern Atlantic Ocean: Deep Sea Drilling Project Initial Reports, v. 44, p. 731-759. CONCLUSIONS Sissingh, W., 1977, Biostratigraphy of Cretaceous calcareous nan noplankton: Geologic en Mijnbouw, v. 56, p. 37-65. Millhaven core samples from 1,077 to 968 ft contain late Campanian Zone CC 22 coccolith floras identified by Sugarman, P.J., Miller, K.G., Bukry, David, and Feigenson, M.D., 1995, Uppermost Campanian-Maestrichtian strontium isoto- key taxa Quadrum trifidum (Stradner) Prins & Perch- pic, biostratigraphic, and sequence stratigraphic framework of Nielsen and Reinhardtites anthophorus (Deflandre) Perch- the New Jersey Coastal Plain: Geological Society of America Nielsen. The consistent presence of Q. trifidum (Stradner) Bulletin, v. 107, p. 19-37. Prins & Perch-Nielsen indicates a warm-water regime simi Thierstein, H.R., 1981, Late Cretaceous nannoplankton and the lar to coeval California floras and unlike cooler water New change at the Cretaceous-Tertiary boundary, in Warme, J.E., Jersey floras. Coccolith species permit direct long-range Douglas, R.G., and Winterer, E.L., eds., The Deep Sea Drill correlation for Georgia floras to paleomagnetic Chron 33n ing Project; a decade of progress: Society of Economic Pale in California and standard European upper Campanian ref ontologists and Mineralogists Special Publication 32, p. 355- erence sections. 394. U.S. Department of the Interior U.S. Geological Survey

Ostracode Biostratigraphy of Upper Campanian (Cretaceous) Marine Sediments from the Millhaven Core, Screven County, Georgia By Gregory S. Gohn

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-E

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract ...... El Introduction ...... 1 Acknowledgments ...... 2 Campanian Marine Deposits in the Millhaven Core ...... 2 Physical Stratigraphy ...... 2 Ostracode Biostratigraphy ...... 3 Ostracode Samples ...... 3 Ostracode Assemblages ...... 4 Biostratigraphy and Age ...... 4 Paleoenvironments ...... 5 Discussion ...... 5 Taxonomic Notes on Ostracodes ...... 6 References Cited ...... 9

PLATE [Plate follows References Cited]

1. Selected Cretaceous ostracodes from the Black Creek Group in the Millhaven core, Screven County, Georgia.

FIGURES

1 . Index map showing location of the Millhaven test hole in Georgia and additional test holes in Georgia and South ...... _ E2 2. Geophysical logs and geologic units of the Cretaceous section in the Millhaven core to a depth of 1,452 feet...... 3 3. Chart showing ostracode interval zones and associated ostracode datums...... 5

TABLE

1. Cretaceous ostracodes from the Black Creek Group in the Millhaven core, Screven County, Georgia...... E4

III

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Ostracode Biostratigraphy of Upper Campanian (Cretaceous) Marine Sediments from the Millhaven Core, Screven County, Georgia

By Gregory S. Gohn

ABSTRACT calcareous nannofossil Zone CC 22 are within the Donoho Creek Formation of the Black Creek Group. The Cretaceous section in the Millhaven core from Screven County, Georgia, contains calcareous, fine-grained INTRODUCTION marine deposits in part of the interval assigned to the Black Creek Group. These calcareous deposits and associated The U.S. Geological Survey (USGS), in cooperation overlying and underlying deposits between depths of 1,119 with the U.S. Department of Energy (USDOE) and the and 927 ft are designated informally as Black Creek subunit Georgia Geologic Survey of the Georgia Department of 2 by Falls and Prowell (this volume, chap. A). Natural Resources, conducted a study of ground-water flow Two informally named ostracode assemblages are and ground-water quality in the area of eastern Georgia that present in Black Creek subunit 2 between depths of 1,043 is adjacent to the USDOE Savannah River Site in South and 975 ft: an older Haplocytheridea everetti assemblage Carolina (fig. 1). This study addressed concerns by the State and a younger Haplocytheridea sarectaensis assemblage. of Georgia regarding the potential for movement of ground The presence of Escharacytheridea pinochii (Jennings) in water containing radionuclides or other contaminants from the lowest studied sample and the presence of Fissocar- the Savannah River Site into Georgia through coastal plain inocythere pidgeoni (Berry) in higher samples indicate a aquifers passing beneath the Savannah River (Clarke, 1992, late Campanian to Maastrichtian age for the interval 1995). between 1,043 and 1,015 ft. This age is compatible with the A principal component of the study was the hydrologic late Campanian age assigned to the calcareous part of Black and geologic analysis of test hole clusters drilled in the Creek subunit 2 by Bukry (this volume, chap. D; calcareous coastal plain sediments of Burke and Screven Counties, Ga. nannofossil Zone CC 22). Both ostracode assemblages are (fig. 1). The hydrologic studies at the cluster sites included strongly dominated by various species of Haplocytheridea determinations of hydraulic properties, pressure heads, and and related genera that suggest inner-neritic paleoenviron- water quality for multiple aquifers (Clarke and others, 1994, ments of deposition for the sediments of Black Creek sub- 1996; Leeth and others, 1996). The geologic studies unit 2. included lithologic, paleontologic, and stratigraphic analy The total range of the ostracode Haplocytheridea ses of the Cretaceous and Cenozoic sediments in continu sarectaensis Brown is within the upper parts of intervals ously cored sections at each site. These geologic analyses assigned to calcareous nannofossil Zone CC 22 in the Mill- were conducted to determine the physical characteristics, haven section and in previously studied test holes in central distributions, and correlations of the several aquifers and South Carolina. The top of Zone CC 22 is slightly older than confining units. This report discusses the ostracode bio- the Campanian-Maastrichtian Stage boundary as defined by stratigraphy, inferred depositional paleoenvironments, and J.A. Burnett and others (1992, Newsletters on Stratigraphy, regional correlation of Cretaceous calcareous marine sedi v. 27, p. 157-172). Hence the highest occurrence of H. ments present in the Millhaven test hole in northern Screven sarectaensis Brown approximates this stage boundary in County, Ga. (fig. 1). eastern Georgia and central South Carolina. Sections in cen The Millhaven stratigraphic test hole was completed tral South Carolina containing H. sarectaensis Brown and by a USGS drill crew in February 1992 to a depth of

El E2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 79'

34° i Sumter i /' Lake Murray c County '^ ,-—' ~" I-, Clark ^H 'Sumter County, \ f(eservo\r~ I sites ,

Savannah ' River \ Lakej Marion / Sjte

St. George MillersT • / Pond Lake Moultrie ^orchester 33C Burke Girard ~i County . County ^ _.- f o ————' "/ r \ Clubhouse --—-(/ /Millhaven'H/ ' *» \ / * --

i^--^~'- Screven ^ —{ County, ^5-..-

ATLANTIC OCEAN

32 C

Figure 1. Location of the Millhaven test hole in Georgia and additional test holes in Georgia and South Carolina.

1,452 ft where the hole bottomed in the Upper Cretaceous Millhaven Cretaceous section. USGS Volunteer-for-Science Cape Fear Formation. This testhole is located in the Burtons Xenedee Bradley assisted in the preparation of the ostra- Ferry Landing 7.5-minute quadrangle in northern Screven code samples from the Millhaven core. I thank Jean M. County at latitude 32°53'25" N., longitude 81°35'43" W. Self-Trail (USGS) for discussions of Cretaceous calcareous (fig. 1). Ground elevation at the drill site is +110 ft. The nannofossils in the South Carolina cores. Reviews by Harry lithologies and stratigraphy of the Millhaven section are dis Dowsett (USGS), Raymond Christopher (Clemson Univer cussed by Clarke and others (1996) and Falls and Prowell sity), and Lucy Edwards (USGS) substantially improved the (this volume, chap. A). manuscript. Depths measured to specific horizons in the Millhaven core typically are 5 to 7 ft deeper than the depths measured to the corresponding positions on the geophysical logs. In CAMPANIAN MARINE DEPOSITS IN THE this report, and throughout this volume, core depths are used MILLHAVEN CORE as the primary depth reference for samples and stratigraphic features. On figure 2, the geophysical logs for the Millhaven test hole have been shifted graphically (down 5 ft) to pro PHYSICAL STRATIGRAPHY duce a closer correspondence between log depths and core depths. Upper Cretaceous sediments are present in the Mill- haven core between its base and a depth of 642 ft (fig. 2) (Falls and others, 1997; Falls and Prowell, this volume, ACKNOWLEDGMENTS chap. A; Edwards and others, this volume, chap. B). Falls and Prowell (this volume, chap. A) assign the interval The site description of the Millhaven core by W. Fred between 1,172 and 839 ft to the Black Creek Group, which Falls (USGS) was an important guide to this study of the they divide into informal lithologic subunits 1, 2, and 3 OSTRACODE BIOSTRATIGRAPHY OF UPPER CAMPANIAN (CRETACEOUS) MARINE SEDIMENTS, GEORGIA E3

Depth Natural gamma log Single-point resistance Geologic units (from base to top). Black Creek subunit 2 (1,119 to 927 ft) contains the only calcareous Cretaceous sediments in the Millhaven core. The calcareous section is present between 1,085 and 940 ft in the core. From its basal contact at 1,119 ft to 1,085 ft, Black Creek subunit 2 consists of noncalcareous, slightly to mod erately muddy, fine to medium, and medium to very coarse sand. This section of sand is broadly gradational upward into calcareous fine-grained deposits that are more typical of the unit. The grain size of the sand fraction and the sand/ (clay+silt) ratio decrease upward in this basal interval. Above 1,085 ft, Black Creek subunit 2 consists of spar ingly calcareous to moderately calcareous, bioturbated, muddy, very fine to fine sand and similar appearing sandy and silty clay. Calcareous macrofossils, microfossils, and nannofossils are present from 1,085 to 965 ft in subunit 2. Molds of pelecypods, locally with traces of preserved cal cium carbonate, are present above 965 to about 940 ft. An interval of slightly muddy, calcareous, very fine to fine sand is present from 1,063 to 1,051 ft. This sand has gradational contacts with underlying and overlying muddier sections. At the top of Black Creek subunit 2, its typically fine-grained deposits grade upward into moderately well-sorted, highly micaceous, very fine to fine sand (934 to 927 ft). The dark, bioturbated, fine-grained sediments of Black Creek subunit 2 in the Millhaven core readily correlate with sections of similar fine-grained marine sediments that are included in the Black Creek Formation or Black Creek Group in wells throughout the Savannah River area (Logan and Euler, 1989; Fallaw and others, 1992a,b; Fallaw and Price, 1992, 1995; Falls and Prowell, this volume, chap. A). Despite their lithologic similarity to Black Creek subunit 2 at Millhaven, few of the correlative Black Creek marine sec tions have retained their calcareous fossils, probably owing to ground-water dissolution of the calcium carbonate.

OSTRACODE BIOSTRATIGRAPHY

OSTRACODE SAMPLES

Twenty-one ostracode samples were collected from the calcareous part of Black Creek subunit 2 in the Millhaven core between depths of 1,082.7 and 940.0 ft. Of these, three TOTAL DEPTH = 1,452 FT samples at the top of the section (965.5, 956.0, and 940.0 ft) did not produce a reaction when treated with dilute hydro Figure 2. Geophysical logs and geologic units of the Cretaceous chloric acid and were assumed to be noncalcareous; these section in the Millhaven core to a depth of 1,452 feet. The samples were not processed. stratigraphic position of Black Creek subunit 2, which was studied for this report, is indicated. The lithostratigraphy is from Falls and The eighteen remaining samples were processed using Prowell (this volume, chap. A). The geophysical logs have been standard microfossil techniques. Samples weighing approx shifted graphically to produce a correspondence between core imately 150 g were soaked in deionized water and sieved. depths and log depths for stratigraphic horizons. Ostracode valves and carapaces were picked from the fine, medium, and coarse sand fractions and placed on standard micropaleontology slides for sorting and identification. E4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Table 1. Cretaceous ostracodes from the Black Creek Group in the Millhaven core, Screven County, Georgia. [Samples are reported as depths (in ft) below the surface]

Haplocytheridea Haplocytheridea sarectaensis assemblage everetti assemblage Species 1,043 1,038 1,033 1,029 ;1,021 1,015 1,010 1,005 1,000 995 989 985 975 Totals % of Total Haplocytheridea sp. aft. H. everetti (Berry) — 0 0 0 0 222 253 11 44 15 31 0 57 0 633 42.9% 0 0 0 0 30 24 8 3 0 4 1 109 16 195 13.2% 166 13 1 0 0 0 0 0 0 0 0 0 0 180 12.2% 30 21 63 5 0 0 0 0 0 0 0 0 0 119 8.1% 0 0 0 0 87 28 1 0 0 0 0 0 0 116 7.9% 72 13 7 1 3 0 0 0 0 0 0 0 0 96 6.5% 16 4 0 0 3 0 0 0 0 0 0 0 0 23 1.6% 0 0 0 0 8 12 0 0 0 0 0 3 0 23 1.6% 2 4 9 0 6 0 0 0 0 0 0 0 0 21 1.4% 0 0 0 0 16 4 0 0 0 0 0 0 0 20 1.4% 16 0 0 0 0 0 0 0 0 0 0 0 0 16 1.1% 5 0 1 0 4 0 0 0 0 0 0 0 0 10 0.7% 0 0 0 1 2 2 0 0 0 0 0 0 0 5 0.3% 1 0 0 0 2 2 0 0 0 0 0 0 0 5 0.3% 5 0 0 0 0 0 0 0 0 0 0 0 0 5 0.3% 0 0 0 0 0 0 0 0 0 0 0 2 0 2 0.1% 2 0 0 0 0 0 0 0 0 0 0 0 0 2 0.1% 0 1 0 0 0 0 0 0 0 0 0 0 0 1 0.1% 0 0 1 0 0 0 0 0 0 0 0 0 0 1 0.1% 0 0 0 0 0 1 0 0 0 0 0 0 0 1 0.1%

Totals —————— ————— ———— 315 56 82 7 383 326 20 47 15 35 1 171 16 1,474 100.0%

Five samples at the bottom of the section (1,082.7, The Haplocytheridea everetti (Berry) assemblage is 1,077.0, 1,067.5, 1,061.5, and 1,051.5 ft) did not yi.eld ostra- dominated by the widel1y distributed sr>ecies Haplo- codes upon processing. Planktonic foraminifers and mol- cytheridea renfroensis Crane and Haplocytheridea everetti lusk fragments also are absent from these five samples; (Berry) as well as undescribed species of the genus Cyther- however, they do contain very sparse assemblages of calcar ella (table 1). These three taxa constitute about 85 percent eous benthic foraminifers, dominantly Lenticulina spp. The of the recovered valves in this assemblage. Brachycythere other thirteen samples produced very small to moderately ovata (Berry), Escharacytheridea pinochii (Jennings), and large numbers of ostracode valves (table 1). These produc typically crushed or fragmented specimens of Loxoconcha tive samples also contain mollusk fragments and calcareous spp. are the only other moderately common forms. Sparse and agglutinated benthic foraminifers. Variable abundances described forms include Curfsina communis (Israelsky), of planktonic foraminifers are present in some of these sam Orthonotacythere hannai (Israelsky), Orthonotacythere sul- ples with heterohelicid genera dominating over globotrun- cata Brown, Antibythocypris fabaformis (Berry), and Fisso- canid genera except at 1,021 and 1,015 ft where carinocythere pidgeoni (Berry). heterohelicids were not seen. The Haplocytheridea sarectaensis Brown assemblage is dominated by Haplocytheridea sarectaensis Brown, Anti bythocypris minuta (Berry), and an undescribed species OSTRACODE ASSEMBLAGES assigned to Haplocytheridea sp. aff. H. everetti (Berry) (table 1). Together, these three species constitute about 93 Two ostracode assemblages are present in Black Creek percent of the assemblage. Sparse described forms include subunit 2 (table 1). The strong dominance of three taxa in Eocytheropteron straillis Brown, Brachycythere rhomboida- each assemblage and the absence or near absence of these lis (Berry), Brachycythere ovata (Berry), Curfsina commu dominant forms in the other assemblage permit definition of nis (Israelsky), and Fissocarinocythere pidgeoni (Berry). the assemblages by inspection.

The lower assemblage, informally named the Haplo BIOSTRATIGRAPHY AND AGE cytheridea everetti (Berry) assemblage, is present in the four samples between the depths of 1,043 and 1,029 ft. The Most of the described species in both Black Creek upper assemblage, informally named the Haplocytheridea ostracode assemblages are long-ranging middle Campanian sarectaensis Brown assemblage, is present in the nine sam to Maastrichtian species or late Campanian to Maastrichtian ples between the depths of 1,021 and 975 ft. species (Crane, 1965; Hazel and Brouwers, 1982; Gohn, OSTRACODE BIOSTRATIGRAPHY OF UPPER CAMPANIAN (CRETACEOUS) MARINE SEDIMENTS, GEORGIA E5

1995). These long-ranging species include Antibythocypris fabaformis (Berry), Antibythocypris minuta (Berry), Regional Selected Brachycythere ovata (Berry), Brachycythere rhomboidalis Stage ostracode (Berry), Haplocytheridea everetti (Berry), Haplocytheridea interval ostracode renfroensis Crane, Curfsina communis (Israelsky) and zones ranges Orthonotacythere hannai (Israelsky). A Two of the described ostracode species in Black Creek subunit 2 can be used to place this section in the regional ostracode zonation of Hazel and Brouwers (1982), as modified by Pitakpaivan and Hazel (1994) (fig. 3). The o CD presence of Escharacytheridea pinochii (Jennings) in the lowest studied sample (table 1), coupled with the presence 'o. CD Veenia of Fissocarinocythere pidgeoni (Berry) in higher samples, Q. 9? indicates placement of at least part of the studied section Q. parallelopora CD (1,043 to 1,015 ft) within the late Campanian to early c 13 "*.05- ^ Maastrichtian chronozones of the Escharacytheridea o pinochii (Jennings) Interval Zone and (or) the Platycosta .c "u_0 C; lixula (Crane) Interval Zone. This late Campanian to early 03 "GO o Maastrichtian age is compatible with the late Campanian o 05 CO age assigned to the calcareous part of Black Creek subunit 2 05 .CO at Millhaven by Bukry (this volume, chap. D) on the basis of LL calcareous nannofossils.

03 03 PALEOENVIRONMENTS O o i_ Q. c Species of the genera Haplocytheridea (Stephenson) CD "CD ^ Platycosta and Antibythocypris (Jennings) tend to dominate the terrige _O lixula 03 ^ nous inner-neritic deposits of the Atlantic and Gulf of Mex CL CD ico Coastal Plains (Hazel and Brouwers, 1982; Puckett, ,03 CD 1996). Conversely, ornate trachyleberid forms and smooth-valved forms (except cytherellids) are more com CD o mon in deeper water chalk and glauconite deposits and tend to be rare in shallow-marine deposits. In the Haplo o cytheridea everetti assemblage (table 1), Haplocytheridea specimens constitute about two-thirds of the recovered "3 valves, and an inner-neritic paleoenvironment is inferred from this assemblage. •S Similarly, in the Haplocytheridea sarectaensis Brown CO assemblage, the abundance of Haplocytheridea specimens O and Antibythocypris minuta (Berry) in moderately diverse •^ ^ CD subassemblages at 1,021 and 1,015 ft suggests an inner-ner Q. Eschara s: itic paleoenvironment. The abundance of two Haplo 05 Q. Q. 13 cytheridea cytheridea species in the higher samples representing this pinochii assemblage and the paucity of other taxa suggest possible 'cCO 1 environmental restrictions during sedimentation in an .^ inner-neritic paleoenvironment, perhaps a low-oxygen water 05 cl. Q. column. E ui 05 O DISCUSSION \ r The relatively little-studied ostracode species Haplo cytheridea sarectaensis Brown holds potential as a local Figure 3. Ostracode interval zones and associated ostracode datums. The ostracode interval zones are from Hazel and biostratigraphic marker. Known occurrences of this species Brouwers (1982) as modified by Pitakpaivan and Hazel (1994). in eastern Georgia and South Carolina are limited to the E6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA upper part of calcareous nannofossil Zone CC 22. Haplo- trated in the literature. Except for a few selected taxa, these cytheridea sarectaensis Brown is present in the interval common species are not illustrated in this report; however, assigned to Zone CC 22 in the Millhaven core (Bukry, this synonymies are provided as a guide to my concepts of these volume, chap. D) and in the USGS-St. George core in north taxa. Brouwers and Hazel (1978) discussed many of the ern Dorchester County, central South Carolina (Self-Trail species listed in these notes; their detailed synonymies pro and Gohn, 1996; for locations, see fig. 1 of this chapter). I vide the bases for many of the synonymies used here. Unde- also have recorded H. sarectaensis Brown at 923 to 898 ft in scribed species listed in table 1 are represented by small the USGS-Clubhouse Crossroads No. 1 core in southern numbers of valves and are not treated in these notes; the sev Dorchester County, which is in a section representing cal eral species representing the smooth-valved genus Cyther- careous nannofossil zone CC 22 (data in Hattner and Wise, ella Jones also are not treated. Listed stratigraphic ranges 1980; J.M. Self-Trail, USGS, 1995, written commun.). In are from Hazel and Brouwers (1982) unless otherwise addition, some specimens from Sumter County, S.C., cores stated. (fig. 1) that I previously assigned to Haplocytheridea wilmingtonensis Brown (in Prowell, 1993, p. 43) are assigned ANTIBYTHOCYPRIS FABAFORMIS (BERRY, 1925) here to H. sarectaensis Brown. These occurrences of H. Cytherellafabaformis Berry, 1925, p. 487, fig. 13. sarectaensis Brown in the Sumter County cores also are within calcareous nannofossil Zone CC 22 (J.M. Self-Trail, Cytheridea fabaformis (Berry, 1925). Alexander, 1929, p. USGS, 1995, written commun.). 76, pi. 5, fig. 18. Burnett and others (1992), Bukry (1994; this volume, Haplocytheridea! fabaformis (Berry, 1925). Schmidt, 1948, chap. D), and Burnett (1996) place the Campanian-Maas- p. 426, pi. 62, fig. 23, text-fig. 2e; Howe and Lauren- trichtian Stage boundary within calcareous nannofossil cich, 1958, p. 350, text-fig.; Benson and Tatro, 1964, p. Subzone CC 23a shortly above the extinction level of Rein- 16, pi. 3, fig. 13; Crane, 1965, p. 199, pi. 1, fig. 11A, B; hardtites anthophorus (Deflandre) Perch-Nielsen at the top Van Nieuwenhuise and Kanes, 1976, pi. 3, fig. B. of Zone CC 22. Therefore, the upper part of calcareous nan Cytheridea (Haplocytheridea) fabaformis (Berry, 1925). nofossil Zone CC 22 is very late Campanian, but not latest Brown, 1957, p. 17, pi. 2, figs. 7, 8; Brown, 1958, p. 58, Campanian, in age. In eastern Georgia and South Carolina, pi. 5, fig. 7. the highest occurrence of Haplocytheridea sarectaensis Antibythocypris fabaformis (Berry, 1925). Brouwers and Brown approximates the top of Zone CC 22 and, hence, Hazel, 1978, p. 25, pi. 2, fig. 8; pi. 3, figs. 1-3; pi. 10, approximates the position of the Campanian-Maastrichtian fig. 5; Hazel and Brouwers, 1982, p. 181, pi. 5, fig. 3; boundary. Gohn, 1995, pi. II, fig. 9. The sections in central South Carolina containing Hap Cythere ulrichi Berry, 1925, p. 483, fig. 3. locytheridea sarectaensis Brown and calcareous nannofossil Zone CC 22 are assigned to the upper part of the Donoho Stratigraphic range.—Middle Campanian through Creek Formation of the Black Creek Group by Gohn Maastricht! an. (1992), Prowell (1993), and Self-Trail and Gohn (1996). Black Creek subunit 2 in the Millhaven core, therefore, ANTIBYTHOCYPRIS MINUTA (BERRY, 1925) occupies the same biostratigraphic position as the upper part Plate 1, figure 3 of the Donoho Creek Formation in central South Carolina; it is also generally similar lithologically to the South Carolina Cytherideis minutus Berry, 1925, p. 487, fig. 12. Donoho Creek sections. As yet, however, Black Creek sub- Cytherideis minuta Berry, 1925. Howe and Laurencich, unit 2 at Millhaven has not been traced lithologically 1958, p. 286. through intervening drill holes to the central South Carolina Antibythocypris minuta (Berry, 1925). Brouwers and Hazel, sections. Although the Donoho Creek Formation is the 1978, p. 25, pi. 3, figs. 4-7; pi. 10, fig. 6; Hazel and uppermost formation in the Black Creek Group in central Brouwers, 1982, p. 184, pi. 4, fig. 2; pi. 5, fig. 13; Gohn, South Carolina (Gohn, 1992; Self-Trail and Gohn, 1996), 1995, pLH, fig. 11. the equivalent section is overlain by a substantial thickness Haplocytheridea! ulrichi (Berry, 1925). Schmidt, 1948, p. of sediments assigned to the Black Creek subunit 3 in the 426, pi. 62, figs. 18, 19; Howe and Laurencich, 1958, p. Millhaven core (fig. 2) (Falls and Prowell, this volume, 358, text-fig.; Crane, 1965, p. 200, pi. 1, fig. 9A, B. chap. A; Frederiksen and others, this volume, chap. C). Cytheridea (Haplocytheridea) ulrichi (Berry, 1925). Brown, 1957, p. 18, pi. 2, figs. 4, 5; Brown, 1958, p. 58, pi. 5, TAXONOMIC NOTES ON OSTRACODES fig- 6. Haplocytheridea! macropora (Alexander, 1929). Schmidt, Most of the described ostracode species listed in table 1948, p. 425, pi. 62, fig. 24; Van Nieuwenhuise and 1 are common, widespread forms that are adequately illus Kanes, 1976, pi. 4, fig. A. OSTRACODE BIOSTRATIGRAPHY OF UPPER CAMPANIAN (CRETACEOUS) MARINE SEDIMENTS, GEORGIA E7

Remarks.—Cythere ulrichi Berry, 1925, is the female CURFSINA COMMUNIS (ISRAELSKY, 1929) dimorph of Antibythocypris fabaformis (Berry, 1925). The Cythereis communis Israelsky, 1929, p. 14, pi. 3A, figs. 9— similar species Antibythocypris macropora (Alexander, 13. 1929) is common in the Gulf of Mexico Coastal Plain but is Cythereis communis Israelsky, 1929. Alexander, 1929, p. rare in the Atlantic Coastal Plain. Antibythocypris minuta 101, pi. IX, fig. 18; Jennings, 1936, p. 52, pi. 7, fig. 3; typically occurs in inner-neritic muddy sands in South Schmidt, 1948, p. 419, pi. 61, figs. 11-13; Skinner, Carolina sections of the Black Creek Group and Peedee For 1956, p. 196, pi. Ill, fig. 7A-£; Butler and Jones, 1957, mation (Self-Trail and Gohn, 1996). p. 35, pi. 3, fig. 6; Howe and Laurencich, 1958, p. 189, Stratigraphic range.—Middle Campanian through text-fig; Crane, 1965, p. 221, pi. 6, fig. 12; Van Nieu Maastrichtian. wenhuise and Kanes, 1976, pi. 2, figs. A, B; Brouwers and Hazel, 1978, pi. 5, figs. 7-9; pi. 10, fig. 8; Smith, BRACHYCYTHERE OVATA (BERRY, 1925) 1978, p. 554, pi. 5, figs. 20-23. Cythereis ovatus Berry, 1925, p. 484, fig. 15. Trachyleberis communis (Israelsky, 1929). Brown, 1957, p. Cythere ovata (Berry, 1925). Alexander, 1929, p. 87, pi. VII, 14, pi. 3, figs. 10, 11; Brown, 1958, p. 63, pi. 4, fig. 5. figs. 10, 13. Trachyleberis? communis (Israelsky, 1929). Benson and Brachycythere ovata (Berry, 1925). Skinner, 1956, p. 190, Tatro, 1964, p. 22, pi. 5, figs. 13-15, text-fig. 10. pi. II, fig. 3A-C; Howe and Laurencich, 1958, p. 89, Curfsina communis (Israelsky, 1929). Hazel and Brouwers, text-figs.; Benson and Tatro, 1964, p. 19, pi. 4, figs. 11- 1982, p. 180, pi. 1, fig. 12; Pitakpaivan and Hazel, 13, text-fig. 6; Crane, 1965, p. 210, pi. 4, fig. 1A, B\ 1994, fig. 3-(4); Gohn, 1995, pi. I, fig. 5. Brouwers and Hazel, 1978, pi. 7, figs. 5-7, pi. 11, fig. Paracythereis semilenis Schmidt, 1948, p. 418, pi. 61, fig. 4; Hazel and Brouwers, 1982, p. 185, pi. 4, fig. 12; 14. Pitakpaivan and Hazel, 1994, fig. 3-(2); Gohn, 1995, pi. Remarks.—Paracythereis semilenis Schmidt, 1948, is II, fig. 2. a molt of Curfsina communis (Israelsky, 1929). Brachycythere ovata vecarina Crane, 1965, p. 210, pi. 4, fig. Stratigraphic range.—Middle Campanian through 3A,fi. Maastrichtian. Cytheropteron sp. A, Israelsky, 1929, p. 7, pi. IA, fig. 1A, C. EOCYTHEROPTERON STRAILLIS BROWN, 1957 Stratigraphic range.—Upper Campanian through Plate 1, figure 6 Maastrichtian. Cytheropteron (Eocytheropteron) straillis Brown, 1957, p. BRACHYCYTHERE RHOMBOIDALIS (BERRY, 1925) 20, pi. 6, figs. 14, 15. Cytheropteron (Eocytheropteron) straillis Brown, 1957. Cythere rhomboidalis Berry, 1925, p. 481, figs. 1, 2. Brown, 1958, p. 60, pi. 7, fig. 14. Cythere rhomboidalis Berry, 1925. Alexander, 1929, p. 86, pi. VII, figs. 1, 2. Stratigraphic range.—Upper Campanian-Maastricht- Brachycythere rhomboidalis (Berry, 1925). Schmidt, 1948, ian (data in Brown, 1957; this report). p. 414, pi. 62, figs. 8-10; Butler and Jones, 1957, p. 28, ESCHARACYTHERIDEA PINOCHII (JENNINGS, 1936) pi. 3, fig. 2A, B; Brown, 1957, p. 11, pi. 4, figs. 5, 8-10; Brown, 1958, p. 61, pi. 2, fig. 9; Howe and Laurencich, Plate 1, figure 5 1958, p. 90, text-figs.; Benson and Tatro, 1964, p. 19, Cytheridea pinochii Jennings, 1936, p. 58, pi. 7, fig. 9. pi. 5, figs. 16-18, text-fig. 7; Crane, 1965, p. 209, pi. 4, Haplocytheridealpinochii (Jennings, 1936). Howe and Lau fig. 7; Van Nieuwenhuise and Kanes, 1976, pi. 2, fig. C; rencich, 1958, p. 356, text-fig. Brouwers and Hazel, 1978, pi. 7, fig. 8; pi. 8, figs. 1-3; Escharacytheridea pinochii (Jennings, 1936). Hazel and pi. 11, fig. 5; Smith, 1978, p. 551, pi. 4, figs. 4-6, 10; Brouwers, 1982, p. 185, pi. 5, fig. 9; pi. 6, fig. 13; Gohn, Hazel and Brouwers, 1982, p. 189, pi. 4, fig. 6; Pitak 1995, pi. Ill, fig. 1; Puckett, 1995, p. 25, pi. 1, figs. 13, paivan and Hazel, 1994, fig. 3-(3); Gohn, 1995, pi. II, 14. fig. I- Brachycythere jerseyensis Jennings, 1936, p. 48, pi. 6, fig. Remarks.—Marker species for the base of the 14A, B. Escharacytheridea pinochii Interval Zone of Hazel and Brouwers (1982). Remarks.—Specimens assigned to Pterygocythere pin- Stratigraphic range.—Upper Campanian and Maas guita Crane,1965 by Crane (1965) and Smith (1978) proba trichtian. bly represent Brachycythere rhomboidalis (Berry, 1925). FISSOCARINOCYTHERE PIDGEONI (BERRY, 1925) Stratigraphic range.—Upper Campanian through Maastrichtian. Cytheridea pidgeoni Berry, 1925, p. 485, figs. 7, 8. E8 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Cythereis pidgeoni (Berry, 1925). Schmidt, 1948, p. 421, pi. HAPLOCYTHERIDEA RENFROENSIS CRANE, 1965 62, figs. 2-6; Howe and Laurencich, 1958, p. 223, Haplocytherideal renfroensis Crane, 1965, p. 201, pi. 2, fig. text-figs.; Crane, 1965, p. 216, pi. 5, fig. 10A, B; Van IA,B. Nieuwenhuise and Kanes, 1976, p. 87, pi. 4, fig. B. Haplocytheridea renfroensis Crane, 1965. Brouwers and Trachyleberis pidgeoni (Berry, 1925). Brown, 1957, p. 14, Hazel, 1978, p. 18, pi. 1, fig. 8; pi. 2, figs. 1, 2; pi. 10, pi. 7, figs. 26, 27; Brown, 1958, p. 63, pi. 4, fig. 3; Ben- fig. 4; Hazel and Brouwers, 1982, p. 189, pi. 4, fig. 17; son and Tatro, 1964, p. 22, pi. 5, figs. 1-3, text-fig. 11. pi. 5, fig. 11; Pitakpaivan and Hazel, 1994, fig. 5-(4). Fissocarinocythere pidgeoni (Berry, 1925). Brouwers and Cytheridea monmouthensis Berry, 1925. Alexander, 1929, p. Hazel, 1978, p. 40, pi. 7, figs. 1^; pi. 11, fig. 3; Hazel 74, pi. 5, figs. 11-14. and Brouwers, 1982, p. 185, pi. 1, fig. 14. Haplocytheridea monmouthensis (Berry, 1925). Swain, "Archicythereis" cf. Cythereis pidgeoni (Berry, 1925). 1952, p. 79, pi. 18, fig. 19; Howe and Laurencich, 1958, Schmidt, 1948, p. 417, pi. 62, fig. 1. p. 355, text-fig. Haplocytheridea? sp. cf. H. monmouthensis (Berry, 1925). Remarks.— "Archicythereis" cf. Cythereis pidgeoni Crane, 1965, p. 200, pi. 1, fig. 12A, B. (Berry, 1925) of Schmidt (1948) is a molt of Fissocar Haplocytheridea? monmouthensis (Berry, 1925). Smith, inocythere pidgeoni (Berry, 1925). Marker species for the 1978, p. 550, pi. 2, figs. 14-16. top of the Platycosta lixula Interval Zone of Pitakpaivan and Haplocytheridea pinochii (Jennings, 1936). Schmidt, 1948, Hazel (1994). p. 427, pi. 61, figs. 25,26. Stratigraphic range.—Upper Campanian and lower Cytheridea plummeri Alexander, 1929. Skinner, 1956, p. Maastrichtian (Hazel and Brouwers, 1982; Pitakpaivan and 197, pi. 4, fig. 2A, D. Hazel, 1994). Haplocytheridea? plummeri (Alexander, 1929). Butler and Jones, 1957, p. 16, pi. 4, fig. 9; Benson and Tatro, 1964, HAPLOCYTHERIDEA EVERETTI (BERRY, 1925) p. 16, pi. 3, figs. 25-27. Cytheridea everetti Berry, 1925, p. 486, fig. 9. Stratigraphic range.—Middle Campanian through Cytheridea everetti Berry, 1925. Alexander, 1929, p. 74, pi. Maastrichtian. 5, figs. 9, 10. HAPLOCYTHERIDEA SARECTAENSIS BROWN, 1957 Haplocytheridea? everetti (Berry, 1925). Howe and Lauren cich, 1958, p. 350, text-fig. Plate 1, figures 1, 2 Haplocytheridea everetti (Berry, 1925). Brouwers and Ha Cytheridea (Haplocytheridea) sarectaensis, Brown, 1957, p. zel, 1978, p. 17, pi. 1, figs. 4, 6, 7, 9; pi. 10, fig. 3; 17, pi. 7, figs. 1-3. Smith, 1978, p. 550, pi. 2, fig. 18; Hazel and Brouwers, Description.—Sexual dimorphism is pronounced. 1982, p. 181, pi. 5, fig. 8; Puckett, 1992, pi. 2, fig. 14. Females have a rounded subtriangular outline and are flat Cytheridea monmouthensis Berry, 1925, p. 486, fig. 10. tened ventrally; the dorsal margin is broadly convex and Cytheridea (Haplocytheridea) monmouthensis (Berry, slightly angled in front of mid-length; the ventral margin is 1925). Brown, 1957, p. 19, pi. 2, fig. 6; Brown, 1958, p. straight in right valves, slightly sinuous in left. Males have 58, pi. 5, fig. 11. elongate-subquadrate outlines; the dorsal margin is very Haplocytheridea monmouthensis (Berry, 1925). Benson and broadly convex; the ventral margin is straight in right Tatro, 1964, p. 16, pi. 6, figs. 17, 21, 23. valves, slightly sinuous in left. The central three-quarters of Cytheridea truncatus Berry, 1925, p. 485, fig. 6. the lateral surface has prominent smooth, low, subvertical ridges that alternate with pitted subvertical furrows. The Haplocytheridea plummeri (Alexander, 1929). Schmidt, longest furrow is slightly in front of the mid-length and is 1948, p. 425, pi. 62, figs. 27-29. convex toward the anterior; the marginal areas of the lateral Cytheridea (Haplocytheridea) plummeri Alexander, 1929. surfaces are smooth. A low node is present near the poste Brown, 1957, p. 18, pi. 2, figs. 9-11. rior-ventral termination in right valves. An indistinct, verti Cytheridea (Haplocytheridea) punctura (Schmidt, 1948). cally elongate node near the anterior margin causes the Brown, 1957, p. 19, pi. 2, figs. 26-28; Brown, 1958, pi. lateral surface to descend steeply to the slanting anterior 5, fig. 11. margin; this node is most pronounced in right valves. The valves have a narrow duplicature and a shallow anterior ves Remarks.—Cytheridea truncatus Berry, 1925 is a juve tibule. The valves have a holomerodont hinge, the anterior nile of Haplocytheridea everetti (Berry, 1925). hinge element is distinctly larger than the posterior ele Stratigraphic range.—Middle Campanian through ment, and the medial element is narrow. Muscle scars are Maastrichtian. not discerned. OSTRACODE BIOSTRATIGRAPHY OF UPPER CAMPANIAN (CRETACEOUS) MARINE SEDIMENTS, GEORGIA E9

Measurements.—Below are measurements (in milli Stratigraphic range.—Middle and upper Campanian meters) of 16 female and 6 male specimens: (Gohn, this report; G. Gohn, unpub. data).

Observed ORTHONOTACYTHERE HANNAI (ISRAELSKY, 1929) Number Average range Cytherideal hannai Israelsky, 1929, p. 12, pi. 2A, fig. Female: 10A, B. Length-———— 16 0.63 0.58-0.67 Cytheropteron hannai (Israelsky, 1929). Alexander, 1929, p. Height--—- 16 0.36 0.33-0.45 105, pi. IX, fig. 16. Male: Orthonotacythere hannai (Israelsky, 1929). Alexander, Length-———— 6 0.75 0.72-0.78 1933, p. 200, pi. 25, fig. 1A-C; pi. 26, fig. 6A, B; pi. 27, Height ----- 6 0.40 0.37-0.43 fig. 14A, B; Skinner, 1956, p. 202, pi. IV, fig. 9A, B; Butler and Jones, 1957, p. 21, pi. 4, fig. 2; Brown, 1957, Comparisons.—The smaller size, pronounced dimor p. 24, pi. 6, figs. 3-5; Brown, 1958, p. 67, pi. 4, fig. 13; phism, and vertical ridges and furrows of Haplocytheridea Howe and Laurencich, 1958, p. 436, text-figs.; Crane, sarectaensis Brown readily distinguish this species from 1965, p. 207, pi. 8, fig. 24; Brouwers and Hazel, 1978, Haplocytheridea everetti (Berry) and Haplocytheridea ren- pi. 9, fig. 4; Smith, 1978, p. 551, pi. 3, fig. 13; Hazel and froensis Crane. Brouwers, 1982, p. 184, pi. 3, fig. 6; Pitakpaivan and Remarks.—As noted by Brown (1957), this species Hazel, 1994, fig. 5-(8). closely resembles early Tertiary species that were later Orthonotacythere (Orthonotacythere) hannai (Israelsky, assigned by Hazel (1968) to the genus Phractocytheridea 1929). Benson and Tatro, 1964, p. 27, pi. 6, figs. 6, 7. Sutton and Williams. In fact, Hazel (1968, p. 131) included Haplocytheridea sarectaensis Brown in Phractocytheridea Stratigraphic range.—Upper Campanian and Maas- Sutton and Williams. However, the Millhaven specimens trichtian (Crane, 1965; Puckett, 1996). appear to lack the strong shelf at the bottom of the anterior ORTHONOTACYTHERE SULCATA BROWN, 1957 socket (left-valve hinge) that was deemed characteristic of Phractocytheridea Sutton and Williams by Hazel (1968). Orthonotacythere sulcata Brown, 1957, p. 23, pi. 6, figs. 6- Therefore, this species is left in Haplocytheridea Stephen- 8. son in this report. At least one of the specimens assigned to Orthonotacythere sulcata Brown, 1957. Brown, 1958, p. 68, Phractocytheridea cf. P. sarectaensis (Brown, 1957) by pi. 4, fig. 14. Puckett (1996, pi. 2, fig. 4) represents the related, more rug Remarks.—This species may be equivalent to Ortho ose species Haplocytheridea wilmingtonensis Brown. notacythere scrobiculata Alexander (Alexander, 1934). Stratigraphic range.—Upper Campanian (data in Stratigraphic range.—Campanian (data in Brown, Brown, 1957; Self-Trail and Gohn, 1996; Gohn, this report). 1957, 1958; Self-Trail and Gohn, 1996).

HAPLOCYTHERIDEA SP. AFF. HAPLOCYTHERIDEA EVERETTI (BERRY, 1925) REFERENCES CITED Plate 1, figure 4 Alexander, C.I., 1929, Ostracoda of the Cretaceous of north Texas: Description.—Valves are moderate sized and subtrian- University of Texas Bulletin 2907, 137 p. gular; males are slightly longer than females. The dorsal ————1933, Shell structure of the ostracode Genus margin is slightly angled in females; the ventral margin is Cytheropteron, and fossil species from the Cretaceous of sinuous in left valves and straight in right valves. The ante Texas: Journal of Paleontology, v. 7, no. 2, p. 181-214. rior margin is broadly rounded and denticulate; denticles are -1934, Ostracoda of the genera Monoceratina and Orthono more abundant on the right valve; the posterior margin is tacythere from the Cretaceous of Texas: Journal of Paleontol rounded and extended. The posterior fifth of the ventral ogy, v. 8, no. 1, p. 57-67. margin is denticulate in the right valve. Node-like thicken Benson, R.H., and Tatro, J.O., 1964, Faunal description of Ostra ings of the left valve occur at the center of the anterior mar coda of the Marlbrook Marl (Campanian), Arkansas: The gin and at the posterior termination; this thickening is most University of Kansas Paleontological Contributions, Article 7, 32 p. pronounced in females. The central two-thirds of the lateral Berry, E.W., 1925, Upper Cretaceous Ostracoda from Maryland: surface has moderate-sized pits; two short, smooth vertical American Journal of Science, v. 9, p. 481-487. ridges at the center are separated and flanked by shallow, Brouwers, E.M., and Hazel, J.E., 1978, Ostracoda and correlation pitted furrows. In right valves, the lateral surface descends of the Severn Formation (Navarroan; Maestrichtian) of Mary at a steep angle to the anterior margin, producing a blunt land: Society of Economic Paleontologists and Mineralogists anterior termination. The anterior vestibule is shallow; the Paleontological Monograph No. 1 (Journal of Paleontology, v. hinge is holomerodont. 52, no. 6, suppl.), 52 p. E10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Brown, P.M., 1957, Upper Cretaceous Ostracoda from North Caro Savannah River Region: Transition between the Gulf and lina: North Carolina Division of Mineral Resources Bulletin Atlantic Coastal Plains: Proceedings of the Second Bald Head 70, 29 p. Island Conference on Coastal Plains Geology, Hilton Head ————1958, Well logs from the Coastal Plain of North Carolina: Island, November 6-11, 1990, University of North Carolina North Carolina Division of Mineral Resources Bulletin 72, at Wilmington, p. 29-32. 68 p. Falls, W.F., Baum, J.S., and Prowell, D.C., 1997, Physical stratig Bukry, David, 1994, Coccolith correlation of Late Cretaceous raphy and hydrostratigraphy of Upper Cretaceous and Pale- Point Loma Formation at La Jolla and Carlsbad, San Diego ocene sediments, Burke and Screven Counties, Georgia: County, California: U.S. Geological Survey Open-File Report Southeastern Geology, v. 36, no. 4, p. 153-176. 94-678, 23 p. Gohn, G.S., 1992, Revised nomenclature, definitions, and correla Burnett, J.A., 1996, Nannofossils and Upper Cretaceous (sub-) tions for the Cretaceous formations in USGS-Clubhouse stage boundaries—State of the art: Journal of Nannoplankton Crossroads #1, Dorchester County, South Carolina: U.S. Geo Research, v. 18, no. 1, p. 23-32. logical Survey Professional Paper 1518, 39 p, 1 pi. in pocket. Burnett, J.A., Hancock, J.M., Kennedy, W.J., and Lord, A.R., ————1995, Ostracode biostratigraphy of the Upper Cretaceous 1992, Macrofossil, planktonic foraminiferal and nannofossil marine sediments in the New Jersey Coastal Plain, in Baker, zonation at the Campanian/Maastrichtian boundary: Newslet J.E.B., ed., Contributions to the paleontology of New Jersey: ters on Stratigraphy, v. 27, no. 3, p. 157-172. Geological Association of New Jersey Contribution Proceed Butler, E.A., and Jones, D.E., 1957, Cretaceous Ostracoda of Pro- ings, v. 12, p. 87-101. thro and Rayburns salt domes, Bienville Parish, Louisiana: Hattner, J.G., and Wise, S.W, Jr., 1980, Upper Cretaceous calcare Louisiana Geological Survey Geological Bulletin 32, 62 p. ous nannofossil biostratigraphy of South Carolina: South Clarke, J.S., 1992, Evaluation of ground-water flow and quality in Carolina Geology, v. 24, no. 2, p. 41-117. the vicinity of the Savannah River Site, Georgia and South Hazel, J.E., 1968, Ostracodes from the Brightseat Formation Carolina [abs.]: Geological Society of America Abstracts (Danian) of Maryland: Journal of Paleontology, v. 42, no. 1, p. with Programs, v. 24, no. 2, p. 9. 100-142. ————1995, Ground-water flow study in the vicinity of the Savan Hazel, J.E., and Brouwers, E.M., 1982, Biostratigraphic and chro- nah River Site, South Carolina and Georgia: U.S. Geological nostratigraphic distribution of ostracodes in the Conia- Survey Fact Sheet FS-178-95, 5 p. cian-Maastrichtian (Austinian-Navarroan) in the Atlantic and Clarke, J.S., Falls, W.F., Edwards, L.E., [Bukry, David,] Frederik- Gulf Coastal Province, in Maddocks, R.F., ed., Texas Ostra sen, N.O., Bybell, L.M., Gibson, T.G., Gohn, G.S., and Flem coda, Guidebook of excursions and related papers for the ing, Parley, 1996, Hydrogeologic data and aquifer Eighth International Symposium on Ostracoda: Houston, interconnection in a multi-aquifer system in coastal plain sed University of Houston, p. 166-198. iments near Millhaven, Screven County, Georgia, 1991-95: Howe, H.V, and Laurencich, L., 1958, Introduction to the study of Georgia Geologic Survey Information Circular 99, 43 p., 1 pi. Cretaceous Ostracoda: Baton Rouge, Louisiana State Univer in pocket. sity Press, 536 p. Clarke, J.S., Falls, W.F, Edwards, L.E., Frederiksen, N.O., Bybell, Israelsky, M.C., 1929, Upper Cretaceous Ostracoda of Arkansas: L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, Arkansas Geological Survey Bulletin 2, p. 3-29. hydrologic and water-quality data for a multi-aquifer system Jennings, PH., 1936, A microfauna from the Monmouth and basal in coastal plain sediments near Millers Pond, Burke County, Rancocas Groups of New Jersey: Bulletins of American Pale Georgia, 1992-93: Georgia Geologic Survey Information Cir ontology, v. 23, no. 78, p. 1-76. cular 96, 34 p., 1 pi. in pocket. Leeth, D.C., Falls, W.F, Edwards, L.E., Frederiksen, N.O., and Crane, M.J., 1965, Upper Cretaceous ostracodes of the Gulf Coast Fleming, R.F., 1996, Geologic, hydrologic, and water-chem area: Micropaleontology, v. 11, no. 2, p. 191-254. istry data for a multi-aquifer system in coastal plain sediments Fallaw, W.C., and Price, Van, 1992, Outline of stratigraphy at the near Girard, Burke County, Georgia, 1992-95: Georgia Geo Savannah River Site, in Fallaw, Wallace, and Price, Van, eds., logic Survey Information Circular 100, 26 p., 1 pi. in pocket. Geological investigations of the central Savannah River area, Logan, W.R., and Euler, G.M., 1989, Geology and ground-water South Carolina and Georgia: Carolina Geological Society resources of Allendale, Bamberg, and Barnwell Counties and Field Trip Guidebook 1992, November 13-15, 1992, part of Aiken County, South Carolina: South Carolina Water Augusta, Georgia, p. B-II-1 to B-II-33. Resources Commission Report 155, 113 p. ————1995, Stratigraphy of the Savannah River Site and vicinity: Pitakpaivan, Kasana, and Hazel, J.E., 1994, Ostracodes and chro- Southeastern Geology, v. 35, no. 1, p. 21-58. nostratigraphic position of the Upper Cretaceous Arkadelphia Fallaw, W.C., Price, Van, and Thayer, PA., 1992a, Cretaceous Formation of Arkansas: Journal of Paleontology, v. 68, no. 1, lithofacies at the Savannah River Site, South Carolina, in p. 111-122. Zullo, V.A., Harris, W.B., and Price, Van, eds., Savannah Prowell, D.C., 1993, Late Cretaceous stratigraphy in the central River Region: Transition between the Gulf and Atlantic Coastal Plain of South Carolina: New evidence from drill Coastal Plains: Proceedings of the Second Bald Head Island holes near Lake Marion, Sumter County: South Carolina Conference on Coastal Plains Geology, Hilton Head Island, Geology, v. 36, p. 35^6. November 6—11, 1990, University of North Carolina at Wilrn- Puckett, T.M., 1992, Distribution of ostracodes in the Upper Creta ington, p. 50-51. ceous (late Santonian through middle Maastrichtian) of Ala ————1992b, Stratigraphy of the Savannah River Site, South bama and Mississippi: Gulf Coast Association of Geological Carolina, in Zullo, V.A., Harris, W.B., and Price, Van, eds., Societies Transactions, v. 42, p. 613-631. OSTRACODE BIOSTRATIGRAPHY OF UPPER CAMPANIAN (CRETACEOUS) MARINE SEDIMENTS, GEORGIA E11

————1995, Planktonic foraminiferal and ostracode biostratigra- Skinner, H.C., 1956, Ostracoda from basal Arkadelphia Marl phy of the late Santonian through early Maastrichtian strata in exposures near Hope, Arkansas: Gulf Coast Association of Dallas County, Alabama: Geological Survey of Alabama Bul Geological Societies Transactions, v. 6, p. 179-204. letin 164, 59 p. Smith, J.K., 1978, Ostracoda of the Prairie Bluff Chalk, Upper Cretaceous, (Maestrichtian) and the Pine Barren Member of ————1996, Ecologic atlas of Upper Cretaceous ostracodes of the Clayton Formation, lower Paleocene, (Danian) from expo Alabama: Geological Survey of Alabama Monograph 14, sures along Alabama state highway 263 in Lowndes County, 176 p. Alabama: Gulf Coast Association of Geological Societies Schmidt, R.A.M., 1948, Ostracoda from the Upper Cretaceous and Transactions, v. 28, p. 539-579. lower Eocene of Maryland, Delaware, and Virginia: Journal Swain, P.M., 1952, Part 2, Mesozoic Ostracoda, chap. B of Ostra of Paleontology, v. 22, no. 4, p. 389^31. coda from wells in North Carolina: U.S. Geological Survey Professional Paper 234, p. 59-93. Self-Trail, J.M., and Gohn, G.S., 1996, Biostratigraphic data for Van Nieuwenhuise, D.S., and Kanes, W.H., 1976, Lithology and the Cretaceous marine sediments in the USGS-St. George No. ostracode assemblages of the Peedee Formation at Burches 1 core (DOR-211), Dorchester County, South Carolina: U.S. Ferry, South Carolina: South Carolina Division of Geology Geological Survey Open-File Report 96-684, 29 p. Geologic Notes, v. 20, no. 3, p. 74-87,

PLATE 1 PLATE 1

[All specimens are selected Cretaceous ostracodes from the Black Creek Group in the Millhaven core from Screven County, Georgia]

Figure 1. Haplocytheridea sarectaensis Brown, 985 ft, exterior view of female right valve (x 90). 2. Haplocytheridea sarectaensis Brown, 985 ft, exterior view of male left valve (x 68). 3. Antibythocypris minuta (Berry), 1,021 ft, exterior view of male left valve (x 73). 4. Haplocytheridea sp. aff. Haplocytheridea everetti (Berry), 1,021 ft, exterior view of female left valve (x 75). 5. Escharacytheridea pinochii (Jennings), 1,043 ft, exterior view of right side of female carapace (x91). 6. Eocytheropteron straillis Brown, 1,015 ft, exterior view of female(?) left valve (x 66). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-E, PLATE 1

'-*>»..

OSTRACODES

U.S. Department of the Interior U.S. Geological Survey

Calcareous Nannofossil Biostratigraphy of Cenozoic Sediments from the Millhaven Core, Screven County, Georgia By Laurel M. Bybell

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-F

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract ...... Fl Introduction ...... 1 Purpose and Scope...... 1 Acknowledgments ...... 1 Material and Methods ...... 1 Biostratigraphic Zonation ...... 2 Millhaven Core ...... 9 Ellenton Formation, Lower and Upper Paleocene, Zones NP 4, NP 5, andNPS ...... 9 Snapp Formation ...... 9 Congaree Formation, Middle Eocene, Zone NP 14 and Possibly Zone NP15 ...... 9 Warley Hill Formation, Middle Eocene, Zone NP 15 and Possibly Zone NP16 ...... 10 Santee Limestone, Middle Eocene, Zone NP 17 and Possibly Zones NP ISorNP 16 ...... 10 Barnwell Unit, Upper Eocene and Possibly Lower Oligocene, Zones NP 19/20-21 ...... 10 GirardCore ...... 11 Millers Pond Core ...... 11 List of Calcareous Nannofossil Species Mentioned in this Paper ...... 11 References Cited ...... 13

PLATE [Plate follows References Cited]

1. Coccolithus, Discoaster, Reticulofenestra, Transversopontis, Helicosphaera, Blackites, Placozygus, Ericsonia, and Toweius.

FIGURES

1. Index map showing the location of the Millhaven, Girard, and Millers Pond test holes in Georgia and additional test holes in South Carolina ...... F2 2. Chart showing calcareous nannofossil biostratigraphic zonation of Cenozoic intervals in the Millhaven core from Georgia ...... 3 3. Calcareous nannofossil occurrence chart for Cenozoic deposits in the Millhaven core from Georgia ...... 4

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Calcareous Nannofossil Biostratigraphy of Cenozoic Sediments from the Millhaven Core, Screven County, Georgia

By Laurel M. Bybell

ABSTRACT the Cretaceous and Cenozoic sediments recovered in the cores. Calcareous nannofossils were examined from the Cenozoic portion of the Millhaven core that was drilled by ACKNOWLEDGMENTS the U.S. Geological Survey in Screven County, Georgia. Calcareous nannofossil Zones NP 4, NP 5, and NP 8 are Donald Queen, Eugene Cobbs, and Eugene Cobbs III, present in the Paleocene Ellenton Formation; calcareous of the U.S. Geological Survey (USGS), drilled the Mill- nannofossils were not examined from the overlying haven corehole, and I thank them for their diligent efforts in noncalcareous Snapp Formation; Zone NP 14 is present in obtaining good core recovery. I thank Jean M. Self-Trail the overlying middle Eocene Congaree Formation; Zone NP (USGS) and Amanda Chapman (USGS) for their prepara 15 occurs in the Warley Hill Formation; Zone NP 17 occurs tion of the calcareous nannofossil samples and their excel in the upper middle Eocene Santee Limestone; and Zone 197 lent illustrations. I also thank Jean M. Self-Trail and 20 and probably Zone 21 occur in the upper Eocene and Raymond A. Christopher (Clemson University) for their possibly lower Oligocene Barnwell unit. A few samples thoughtful reviews of the manuscript. were examined from the Ellenton Formation in the core from the nearby Girard test hole and the Santee Limestone in the Millers Pond core. These samples could add no more MATERIAL AND METHODS precise information concerning the age of these two formations. The Millhaven test hole (33X048) was drilled in Screven County, Ga., in late 1991 and early 1992 as part of a cooperative effort among the U.S. Geological Survey, the INTRODUCTION U.S. Department of Energy, and the Georgia Geologic Sur vey of the Georgia Department of Natural Resources. The test hole is located at lat 32°53'25" N. and long 81°35'43" PURPOSE AND SCOPE W. (fig. 1). The drill site is located at an altitude of 110 ft, and the test hole was drilled to a depth of 1,452 ft. The hole In this study, calcareous nannofossils were examined was continuously cored, and the cores are temporarily from 68 samples from the Cenozoic portion of the Mill- stored at the U.S. Geological Survey in Reston, Va. haven core in order to establish a biostratigraphic frame Sixty-eight samples between the depths of 639.6 and work that could be used to understand better the ground- 59.8 ft in the Millhaven core were examined for their calcar water flow in the aquifers in the region near the Savannah eous nannofossil content (fig. 2). Two samples were exam River Site. I anticipated that calcareous nannofossils would ined from the Girard core (32Y020), which was drilled by not be useful in dating the more updip Girard and Millers the U.S. Geological Survey in 1992 in southern Burke Pond test holes, but I examined a few select samples in County, Ga., at the lookout tower on Griffins Landing Road, order to test this hypothesis. Falls and Prowell (this volume, 2 miles north of the town of Girard at lat 33°03'54" N. and chap. A) describe the lithology and physical stratigraphy of long 81°43'13" W. (fig. 1). Three samples were examined Fl F2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 81' 80' 79'

34°

33C

ATLANTIC OCEAN

32C 0 20 Miles

0 20 Kilometers

Figure 1. Location of the Millhaven, Girard, and Millers Pond test holes in Georgia and additional test holes in South Carolina. from the Millers Pond core (GGS-3758, Burke 2), which that bonds glass to glass and cures when exposed to ultra was drilled by the Georgia Geologic Survey in 1991 in violet radiation. northern Burke County, Ga., 2 miles west of the Savannah Initially, all samples were examined by using a Zeiss River and 16 miles south of Augusta at lat 33°13'48" N. and Photomicroscope III. A few samples, which were thought to long 81°52'44" W. (fig. 1). Comparisons are made with cal have the best preservation and the highest abundances of careous nannofossil data obtained from the Clubhouse calcareous nannofossils, were scanned by using a JEOL 35 Crossroads core No. 1 (Hazel and others, 1977) and the scanning electron microscope (SEM). Photomicrographs of Pregnall core (Edwards and others, 1997), both located in several of the best preserved specimens are presented on Dorchester County, S.C. plate 1. Calcareous nannofossil samples were extracted from the central portion of core-segment surfaces (freshly broken where possible) at approximately 2- to 10-ft intervals. The BIOSTRATIGRAPHIC ZONATION samples were dried in a convection oven to remove residual water, and the resultant sediment was placed in vials for In this study, the biostratigraphic zonation of the Ceno- long-term storage in the author's laboratory at the U.S. Geo zoic strata is based primarily on the calcareous nannofossil logical Survey in Reston, Va. A timed settling procedure zonation of Martini (1971) and secondarily on the zonation was used to obtain the optimum sediment-size fraction. For of Bukry (1973, 1978) and Okada and Bukry (1980). The this procedure, a small amount of sample was placed in a calcareous nannofossil assemblages usually were sufficient beaker, stirred, and settled through 2 cm of water. The first in numbers of specimens, diversity of taxa, and preserva- tional state in the Millhaven strata to allow placement of settling time was 1 minute to remove the coarse material, most samples within one specific calcareous nannofossil and the second settling time was 10 minutes to remove the zone (fig. 3). fine clay fraction. Smear slides then were prepared from the remaining material. Cover slips were attached to the slides using Norland Optical Adhesive (NOA-65), a clear adhesive Text continues on p. F8. CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA F3

100 -

EXPLANATION

Fossils 200 - t Calcareous sand

^-^^-2 Clay

Clayey sand 300 - I \

Sand 1 u Sandy limestone

Limestone 400 -

ZZT Clayey limestone

Calcareous clay

500 - Calcareous nannofossil sample

? Uncertain age

600 -i_-^_-^_-^_ Figure 2. Calcareous nannofossil biostratigraphic zonation of Cenozoic intervals in the Millhaven core from Georgia. Lithology and formations from Falls 642 NP4 and Prowell (this volume, chap. A). F4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Ellenton Formation Congaree Fm. Warley Hill Formation

Early Paleocene Late Paleocene Middle Eocene '/">'/">'<~>>n'<~>'/">'<~> .3 •*'*'* l/")l/")l/")l/")l/")tOV")l/")l/")l/~)l/")l/") 00 00 OH OH OH ^0-0-^^Î^Ô-aHâH OH OH O.QHQHQHQHO-QHQHQ-QHQHQHO-QHO- 1 z, z, z ZZZZZZZZZZ.ZZ Z, Z, 'ZZZ.Z.ZZZZZZZZZZZ JH "cL C-1 v£> 00 Tf ro^cN — oo^HvoÔOiriCN O CN •^lOtoioioO^ÔrîoioioiooO o\ *o in T-ÔO^HC^ÔNlOrÔN^H^^ oo r- în — roincNooÔrocNiriÔOro^- V fc r^ r*^ r^ f>fSr)i— lOONONONOOoor-r- r- i^ GNGNOOO^DÔtOlO-^Tfr^CNCN^HO Species o ^c « « *CvO*C*CvOn u~> •«t'«t 1*'«t'«tTj-Tj--^-'«J-^-Tj-Tj-Tj-Tj-^J-

X . X . . . X . X X X X xxxxxxxxxxxxxxx

xxxx.x.x.xxx X X XXXXXXXXX. . . .XX

1 ...... X

X . XXX . XXXXXXXXX . . 2 ...... c . . x.xxx.x.x. .xxxx X . X xxxx.x.x.x.x X X xxxxxxxxxxxxxxx C . . c ......

x X X ^ ^ xxxxxxxxxxxxxxx

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X 1 ...... 311 1

J£

XXX xxxx. . .x.xxx X X

Gonlolithus fluckigeri ————————— Hayella situliformis —— - -——— - — — — Helicosphaera bramlettei ——————— . . . . 1 ...... Helicosphaera compacta ——————

Helicosphaera lophota ———————— Helicosphaera reticulata ———————

Figure 3. Calcareous nannofossil occurrence chart for Cenozoic deposits specimen in greater than 10 fields of view at x 500; B, barren of calcareous in the Millhaven core from Georgia. The following symbols are used. nannofossils. Preservation: F, fair; P, poor; T, terrible. Other symbols: Abundance: A, abundant or greater than 10 specimens per field of view at 1,2,3, only one, two, or three specimens observed in entire sample; C, x 500; C, common or 1 to 10 specimens per field of view at x 500; F, contaminated specimen from elsewhere; 7, possible occurrence. frequent or 1 specimen per 1 to 10 fields of view at X 500; R, rare or 1 CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA F5

Santee Limestone Barn well unit Late Eocene/ Middle Eocene Late Eocene Early Oligocene

*£> *£> *£> ooooooooorirtrj- _. CJ C2 CJ CJ CJ C2 CJ CJ CJ i ^ ^ \ \ e~ f~ ^^^^.-^ —i — ^^H —i r-i — ^^^-H^^c^(NtN(N CL, CL, CL, 1X1X1X1X1X1X1X1X1X0.1X1X0, z z z ^. c- zzzizzzzzzizzzz ZZ,&Z,Z,Z,Z,ZZ,Z,Z,Z,%Z,Z,Z,r-r- oooooo\oooooo>nooomo>n>n o\ooo>ntNOoo>nooooo'n Ocooo oôo\/'>mvooO'-«mcôôoonôooO'-^'-ôo>nco lx,.^ 0< oo\r^t^r^ô^£>>n^tmm'-ôo\'n^t^tcv| nmrt005?S?i •*±mmmcococommcocommcNcNcNcNcN r~lr~l(N(Nr~lr~l^^-H^^^rt-H^ ON ^3u ' Species

X ...... Blackites tenuis

X.I...... 1 ......

Chiasmolithus consuetus s.l.

Chiasmolithus grandis ...... 1 ...... Chiasmolithus oamaruensis

XXX. .XXXX.XXXXX. .X XXXXXXXXX. . . .XXX. Coccolithus pelagicus

Cruciplacolithus tenuis Cruciplacolithus spp.

XXX. .XXXX.XXXX.X.X XXXXXXXXX. . .XXXX. Cyclococcolithus formosus X X Cyclococcolithus spp. X.X.XXX. . . .X XXXXXXXXX. . . .XXX. Dictyococcites bisectus Dictyococcites scrippsae

Discoaster mirus Discoaster saipanensis Discoaster sublodoensis Discoaster tanii

Ellipsolithus macellus Ericsonia obruta

Helicosphaera bramlettei

...... 1 ...... Helicosphaera reticulata Figure 3. Continued. F6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Ellenton Formation Congaree Fm. Warley Hill Formation Early Paleocene Late Paleocene Middle Eocene u in in ^o a o •^••^•^-•^•^^y-ju-jininininininin N •* •«!• •«!• inininin'n'ninin'nininin 00 OO a. CM OH PL, 0.0.0.1X0.0.0.0.0.0.0.0. ooooooooooooooo 2; 2 2; ZZZZZZZZZZZZ 1

tc- ô oo TJ- rorêNi— ioo^H\or~OOc-J O CM •^tmininino — omminminoo o ô in ^HOO*-^roc7\QNinroc7N^-io> OO f~ t^m^Hrnin(NooômcsinÔOrori- o • «J 5tJ m ro m PICSC-)'— ioo\o\o\oooor~r~ p~ p~ o\iôoi^\oôininT)-TtmcscM^-io species Q \o \o ô « ôinininininmin

2 2

X . X

Prinsius spp. ———————————— X Pseudotriquetrorhabdulus inversus ———

C . . x.xxxxxxx. .xxxx c ...... XX. .X.X.X. .XXXX c . .

XXX. XXX. XXXX. X.

X X X

X . X XX. X. . .X.XXX X X

. . 3 ......

Transversopontis pulchriporus ————— Transversopontis zigzag — —— - ——— — X XXXXXXXXXX . XXXX

Cretaceous forms —————————— X . X X X X ...... F R F FFRFRRRFBRFF F F- FRFCFFCFCCCFCFF P T F pppppppp p p F F P FPPFPPPPPPPFFPF

The Snapp Formation was cored above the Ellenton Formation from 504 to 570 ft; the Snapp did not yield any calcareous nannofossil samples.

Figure 3. Calcareous nannofossil occurrence chart for Cenozoic deposits specimen in greater than 10 fields of view at x 500; B, barren of calcareous in the Millhaven core from Georgia. The following symbols are used. nannofossils. Preservation: F, fair; P, poor; T, terrible. Other symbols: Abundance: A, abundant or greater than 10 specimens per field of view at 1,2,3, only one, two, or three specimens observed in entire sample; C, x 500; C, common or 1 to 10 specimens per field of view at x 500; F, contaminated specimen from elsewhere; ?, possible occurrence— frequent or 1 specimen per 1 to 10 fields of view at x 500; R, rare or 1 Continued. CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA F7

Santee Limestone Barnwell unit Late Eocene/ Middle Eocene Late Eocene Early Oligocene ^c ^o ^o cjcjcjcjcjcjcjcjcd77777^^-ooooooooorjzjr;^ _

—— —— ^H^H^^^.,—— ^H^H^Hrt^HCNtNfNtN

OH OH OH ^(^(^(^e^!^^^^^^^^ &,&,&,&,&,&,&,&,&,&,&,&,&<&,&,&< zzz^. ^.zzzzz^zzzzzzz ZZZZZZZZZZZ^ZZZZ^-^'

OOOOOO\OOOOOOW)OOOinOW>W> o\ooo>nr)ooo'nooooo'n Ocr)00 OÔO\i/ioooir>ir>vooo — r^tôÔootNt^ lOcnONVOfSOioÔooo-H-HOOiocnuûô: O(^t^t^t^Ô^»n^trnm — ôîrj^f^tfN r<->~HOOo?5g|£ rfencnrrienfênf^c^fOfnencnc^tSfSMfS (N(N(N(N

X Poniosphaera punctosa Pontosphaera wechesensis

XXXX.XX. .X. .X XXXXXXXX. . . . .XXX. Reticulofenestra umblicus

Sphenolithus pseudoradians X ......

X X

XX X XXX X

XXX. .XXXX.XXXX. . .X XXXXXXXXX. . . . .XX. Zygrhablithus bijugatus placoliths Cretaceous forms CFFBRFCFFRFCFFFFBF ACCFCCCFRBRBRFFCBB Abundance PPP PPFPPPPPPPPP F FFPPFPPPP P PPPP Preservation Figure 3. Continued. F8 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

The following calcareous nannofossil species can be FAD *#Nannotetrina fulgens (Stradner) Achuthan & used to date sediments of early Paleocene to early Oli- Stradner—base of Zone NP 15, base of Sub- gocene age. Many, but not all, of these species are present in zone CP 13a, middle Eocene, the genus Nan- the Millhaven core. A FAD indicates a first appearance notetrina first appears very near the Zone NP datum, and a LAD indicates a last appearance datum. Zonal 14/15 boundary markers for the Martini NP zones are indicated with an LAD *Rhabdosphaera inflata Bramlette & Sullivan— asterisk (*), and a pound sign (#) indicates a zonal marker top of Zone NP 14, base of Subzone CP 12b, for the Bukry CP zones. The author has found the remaining middle Eocene species to be biostratigraphically useful in the Gulf of Mex- FAD *Rhabdosphaera inflata Bramlette & Sullivan— ico and Atlantic Coastal Plains (Bybell, 1982; Bybell and middle of Zone NP 14, top of Subzone CP Gibson, 1985; Poore and Bybell, 1988; Self-Trail and 12b, middle Eocene Bybell, 1995). FAD *#Discoaster sublodoensis Bramlette & Sullivan— LAD *#Reticulofenestra umbilicus (Levin) Martini & base of Zone NP 14, base of Subzone CP Ritzkowski—top of Zone NP 22, top of Sub- 12a, early Eocene zone CP 16c, early Oligocene LAD *Rhomboaster orthostylus (Shamrai) Bybell & LAD *Cyclococcolithus formosus Kamptner—top of Self-Trail—top of Zone NP 12, early Eocene Zone NP 21, early Oligocene FAD Helicosphaera lophota (Bramlette & Sullivan) LAD Isthmolithus recurvus Deflandre—within Zone NP Locker—near top of Zone NP 12; has been 21 used to approximate the Zone NP 12/NP 13 LAD *#Discoaster saipanensis Bramlette & Riedel— boundary, early Eocene top of Zone NP 19/20, top of Subzone CP FAD Helicosphaera seminulum Bramlette & Sullivan— 15b, late Eocene middle of Zone NP 12, early Eocene LAD #Discoaster barbadiensis Tan Sin Hok—top of FAD *Discoaster lodoensis Bramlette & Riedel—base Zone NP 19/20, top of Subzone CP 15b, late of Zone NP 12, early Eocene Eocene; actually has its LAD slightly below LAD *#Rhomboaster contortus (Stradner) Bybell & the LAD of D. saipanensis Self-Trail—top of Zone NP 10, top of Sub- LAD Cribrocentrum reticulatum (Gartner & Smith) zone CP 9a, early Eocene Perch-Nielsen—very near top of Zone NP FAD *Rhomboaster bramlettei (Bronnimann & Strad 19/20, late Eocene ner) Bybell & Self-Trail—base of Zone NP FAD ^Isthmolithus recurvus Deflandre—base of Zone 10, early Eocene NP 19/20, late Eocene FAD *#Discoaster multiradiatus Bramlette & Riedel— FAD *#Chiasmolithus oamaruensis (Deflandre) Hay et base of Zone NP 9, base of Subzone CP 8a, al.—base of Zone NP 18, base of Subzone late Paleocene CP 15a, late Eocene FAD *Heliolithus riedelii Bramlette & Sullivan—base FAD Helicosphaera compacta Bramlette & Wilcoxon— of Zone NP 8, late Paleocene within the uppermost part of Zone NP 16; FAD *#Discoaster mohleri Bukry & Percival—base of can be used to approximate the Zone NP 16/ Zone NP 7, base of Zone CP 6, late Pale 17 boundary. ocene LAD *#Chiasmolithus bidens (Bramlette & Sullivan) FAD *#Heliolithus kleinpellii Sullivan—base of Zone Hay & Mohler/Chiasmolithus solitus (Bram NP 6, base of Zone CP 5, late Paleocene lette & Sullivan) Hay et al.—top of Zone NP FAD Heliolithus cantabriae Perch-Nielsen—within 16, middle Eocene upper part of Zone NP 5, late Paleocene FAD Cribrocentrum reticulatum (Gartner & Smith) FAD Chiasmolithus bidens (Bramlette & Sullivan) Hay Perch-Nielsen—within Zone NP 16, middle & Mohler—within Zone NP 5, late Pale Eocene ocene FAD Dictyococcites bisectus (Hay et al.) Bukry & Per- FAD *#Fasciculithus tympaniformis Hay & Mohler— cival—within Zone NP 16, middle Eocene base of Zone NP 5, base of Zone CP 4, late FAD Dictyococcites scrippsae Bukry & Percival— Paleocene within Zone NP 16, middle Eocene FAD Chiasmolithus sp. aff. C. bidens (Bramlette & Sul FAD #Reticulofenestra umbilicus (Levin) Martini & livan) Hay & Mohler—within Zone NP 4 Ritzkowski—large forms first appear near FAD Toweius pertusus (Sullivan) Romein—within Zone base of Zone NP 16, base of Subzone CP NP4 14a, middle Eocene FAD Ellipsolithus distichus (Bramlette & Sullivan) Sul LAD *Rhabdosphaera gladius Locker—top of Zone NP livan—near base of Zone NP 4, early Pale 15, middle Eocene ocene CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA F9

FAD *#EUipsolithus macellus (Bramlette & Sullivan) and others, 1985, 1995). Calcareous nannofossils cannot be Sullivan—base of Zone NP 4, base of Zone used to determine whether the samples from the Millhaven CP 3, early Paleocene core are in the lower or upper part of Zone NP 4. However, FAD *#Chiasmolithus danicus (Brotzen) Hay & dinoflagellates (Edwards, this volume, chap. G) and fora- Mohler—base of Zone NP 3, base of Zone minifers (Gibson, this volume, chap. I) clearly place this CP 2, early Paleocene interval within the early Paleocene. For example, the plank- FAD *#Cruciplacolithus tenuis (Stradner) Hay & tonic foraminifer Globoconusa daubjergensis (Bronni- Mohler—base of Zone NP 2, base of Sub- mann), which occurs at 636.8 ft, never occurs in material zone CP Ib, early Paleocene younger than the lower Paleocene (Gibson, this volume, chap. I). Calcareous nannofossil contamination normally is The 12 samples from 631.3 to 579.2 ft are placed confined to occasional reworked specimens of Cretaceous within the lower part of Zone NP 5 (late Paleocene) by the species. However, at 639.6 ft in the Millhaven core, there is presence of Chiasmolithus bidens (Bramlette & Sullivan) a significant amount of downhole contamination of middle Hay & Mohler (FAD within Zone NP 5) and the absence of Eocene calcareous nannofossil specimens into a highly both Heliolithus cantabriae Perch-Nielsen (FAD in upper porous middle Paleocene sample. This is presumed to be the half of Zone NP 5) and Heliolithus kleinpellii Sullivan (FAD result of injection into open spaces of material from farther defines the base of Zone NP 6). Fasciculithus tympaniformis up in the corehole via drilling fluid. Contamination of Hay & Mohler (FAD defines the base of Zone NP 5) is rare Eocene pollen also was observed in this interval (see Fred- in the Millhaven core and could not be used as a reliable eriksen, this volume, chap. H). Two samples in the Pregnall biostratigraphic indicator. An unconformity within the core in Dorchester County, S.C., also are contaminated with Ellenton Formation comprises the upper part of Zone NP 4. middle Eocene calcareous nannofossils (Edwards and oth Two samples from 578.0 and 577.2 ft are placed in the ers, 1997), but there the contamination occurs in porous late Paleocene Zone NP 8 on the basis of the presence of upper Paleocene limestone rather than in the middle Pale Heliolithus riedelii Bramlette & Sullivan (FAD defines the ocene section. The possibility for this type of contamination base of Zone NP 8) and the absence of Discoaster multira- is always present when dealing with cores, but careful sam diatus Bramlette & Riedel (FAD defines the base of Zone pling procedures and awareness that contamination is possi NP 9). An unconformity in the Ellenton spans the upper part ble can reduce significantly the chances for biostratigraphic of Zone 5 and Zones NP 6-7. No calcareous nannofossil dating errors. samples were collected from the upper 7 ft of the Ellenton Formation. It is unknown whether there might be material of MILLHAVEN CORE Zone NP 9 age (uppermost Paleocene) in this interval. Zone NP 9 is present in Dorchester County, S.C., both in the Preg nall core (Edwards and others, 1997) and in the Clubhouse ELLENTON FORMATION, Crossroads No. 1 core (Hazel and others, 1977). LOWER AND UPPER PALEOCENE, ZONES NP 4, NP 5, AND NP 8 SNAPP FORMATION Sediments in the interval from 642 to 570 ft in the Calcareous nannofossils were not examined from the Millhaven core are placed in the Ellenton Formation (Falls noncalcareous Snapp Formation, which extends between and Prowell, this volume, chap. A). Seventeen samples from 570 and 504 ft in the core. See Frederiksen (this volume, 639.6 to 577.2 ft in this unit were examined for their calcar chap. H) for a discussion of the pollen from the Snapp For eous nannofossil content (fig. 3). mation. Three samples from 639.6, 636.8, and 635.4 ft are placed in Zone NP 4 because of the presence of Ellip- solithus macellus (Bramlette & Sullivan) Sullivan (FAD CONGAREE FORMATION, defines the base of Zone NP 4) and Chiasmolithus sp. aff. C. MIDDLE EOCENE, ZONE NP 14 bidens (Bramlette & Sullivan) Hay & Mohler, which occurs AND POSSIBLY ZONE NP 15 only within Zone NP 4, and the absence of species indica tive of Zone NP 5. The central X-shaped structure of C. sp. Five samples were examined from the Congaree For aff. C. bidens closely resembles that of Chiasmolithus mation, which extends from 504 to 462 ft in the Millhaven bidens (Bramlette & Sullivan) Sullivan, except that the X is core (fig. 3). Four samples from 497.4, 495.5, 481.5, and unsplit. Perch-Nielsen (1985) contains a discussion of split 473.5 ft can be placed in Zone NP 14 by the presence of versus unsplit terminology for the genus Chiasmolithus. Discoaster sublodoensis Bramlette & Sullivan (FAD defines Lower Zone NP 4 is placed in the early Paleocene, and the base of Zone NP 14) at 497.4, 495.5, and 481.5 ft; the upper Zone NP 4 is placed in the late Paleocene (Berggren presence of Rhabdosphaera inflata Bramlette & Sullivan F10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

(only occurs in the upper part of Zone NP 14) at 473.5 ft; At 368.0 ft, the sample does contain frequent calcare and the absence of the genus Nannotetrina (FAD at the base ous nannofossils and a moderate assemblage with 21 spe of Zone NP 15) in this material. Discoaster saipanensis cies present. The absence of Chiasmolithus bidens Bramlette & Riedel (early forms of this species first appear (Bramlette & Sullivan) Hay & Mohler/Chiasmolithus soli in Zone NP 14), Lanternithus minutus Stradner (first tus (Bramlette & Sullivan) Hay et al. is considered to be sig appears in the upper part of Zone NP 14), and Lithostroma- nificant, and this sample is placed in Zone NP 17. The 11 tion operosum (Deflandre) Bybell and Lithostromation sim samples in the interval from 365.0 to 242.5 ft also are placed plex (Klumpp) Bybell (both first appear in Zone NP 14) are in Zone NP 17 because of the absence of Chiasmolithus present in this interval. The sample at 473.5 ft, which is def bidens (Bramlette & Sullivan) Hay & Mohler/Chiasmo initely in the upper part of Zone NP 14 because of the pres lithus solitus (Bramlette & Sullivan) Hay et al. (LAD at the ence of Rhabdosphaera inflata Bramlette & Sullivan, is top of Zone NP 16) and the presence of Helicosphaera com- middle Eocene in age. The absence of R. inflata Bramlette pacta Bramlette & Wilcoxon (FAD very near the top of & Sullivan in the lower three samples could indicate that Zone NP 16), Reticulofenestra umbilicus (Levin) Martini & these samples are from the lower part of Zone NP 14 (upper Ritzkowski, Cribrocentrum reticulatum (Gartner & Smith) part of the early Eocene) or, more probably, the absence is Perch-Nielsen, Dictyococcites bisectus (Hay et al.) Bukry & the result of poor calcareous nannofossil assemblages in Percival, and Dictyococcites scrippsae Bukry & Percival these samples. The sample from 465.5 ft contains no diag (FAD's in Zone NP 16). nostic species and could be in either Zone NP 14 or Zone NP15. BARNWELL UNIT, UPPER EOCENE AND POSSIBLY LOWER WARLEY HILL FORMATION, OLIGOCENE, ZONES NP 19/20-21 MIDDLE EOCENE, ZONE NP 15 AND POSSIBLY ZONE NP 16 Nineteen samples were examined from the Barnwell unit between 227.5 and 59.8 ft in the Millhaven test hole. Ten samples were examined from the Warley Hill For The lowest calcareous nannofossil sample from the Barn- mation, which extends from 462 to 401 ft in the Millhaven well unit at 227.5 ft tentatively has been placed in the mid core (fig. 3). The lowest sample from 462.0 ft can be dated dle Eocene Zone NP 17 because it overlies material of Zone no closer than either Zone NP 14 or Zone NP 15. Eight sam NP 17 age but contains no species indicative of a younger ples from 458.1 to 413.0 ft are placed in Zone NP 15 age. The fact that the rest of the Barnwell unit is in the late because of the presence of Chiasmolithus gigas (Bramlette Eocene (Zone NP 19/20 or younger) indicates that this sam & Sullivan) Hay et al. (FAD and LAD in Zone NP 15) in ple most likely is also of late Eocene age, and the age dis this interval and because large specimens of Reticulofenes- crepancy is the result of the absence of diagnostic late tra umbilicus (Levin) Martini & Ritzkowski (FAD near the Eocene species in the sample. The author has observed sim base of Zone NP 16) are not present. The sample from 404.0 ilar discrepancies near formational contacts elsewhere in the ft can be no older than Zone NP 15 because it overlies sedi Gulf of Mexico and Atlantic Coastal Plains. ments of this age and can be no younger than Zone NP 16 The nine samples that were examined from 225.9 to because it contains Chiasmolithus bidens (Bramlette & Sul 168.5 ft are placed in Zone NP 19/20 because of the pres livan) Hay & Mohler/Chiasmolithus solitus (Bramlette & ence of Isthmolithus recurvus Deflandre (FAD defines the Sullivan) Hay et al. (LAD defines the top of Zone NP 16). base of Zone NP 19/20), Discoaster saipanensis Bramlette & Riedel (LAD defines the top of Zone NP 19/20), Dis SANTEE LIMESTONE, coaster barbadiensis Tan Sin Hok, and Cribrocentrum retic MIDDLE EOCENE, ZONE NP 17 AND POSSIBLY ulatum (Gartner & Smith) Perch-Nielsen (LAD's very near ZONES NP 15 OR NP 16 the top of Zone NP 19/20). The three samples from 160.0, 151.0, and 131.0 ft can be dated no more accurately than Seventeen samples were examined from the Santee Zone NP 19/20 or Zone NP 21. This is because the samples Limestone, which extends from 401 to 228 ft in the Mill- from 160.0 and 131.0 ft are barren of calcareous nannofos haven core (fig. 3). The deepest three samples from 400.0 to sils and the sample at 151.0 ft contains only rare and poorly 379.8 ft tentatively are placed in Zones NP 15 or NP 16 preserved specimens. because they contain Chiasmolithus bidens (Bramlette & Four samples at 118.0, 105.0, 103.5, and 95.0 ft ques Sullivan) Hay & Mohler/Chiasmolithus solitus (Bramlette tionably are placed in Zone NP 21. All four samples contain & Sullivan) Hay et al. (LAD defines the top of Zone NP 16) Isthmolithus recun>us Deflandre (FAD at the base of Zone and overlie samples of Zone NP 15 age. The sample from NP 19/20 and LAD in Zone NP 21) and Cyclococcolithus 375.0 ft is barren of calcareous nannofossils, and the sample formosus Kamptner (LAD defines the top of Zone NP 21). from 370.9 ft contains only rare nondiagnostic species. Also, all four samples do not have Discoaster barbadiensis CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA Fl 1

Tan Sin Hok, Discoaster saipanensis Bramlette & Riedel, or Transversopontis pulcheroides (Sullivan) Baldi-Beke Cribrocentrum reticulatum (Gartner & Smith) Perch- Transversopontis zigzag Roth & Hay Nielsen (LAD's near or at the top of Zone NP 20). However, Zygrhablithus bijugatus (Deflandre) Deflandre the absence of all but one specimen of the genus Discoaster in this interval could possibly indicate that Discoaster bar- The age of the sample at 120 ft is middle to late badiensis Tan Sin Hok and Discoaster saipanensis Bram Eocene, and unfortunately cannot be constrained any closer lette & Riedel are absent for other than evolutionary than Zones NP 16 to NP 21. The highest sample at 82 ft was reasons. There is a possibility that this material is still in barren of calcareous nannofossils. Zone NP 19/20. The Eocene/Oligocene boundary occurs within Zone NP 21 (Berggren and others, 1985, 1995). So if this interval in the Millhaven core is in Zone NP 21, it could LIST OF CALCAREOUS NANNOFOSSIL be either late Eocene or early Oligocene in age. SPECIES MENTIONED IN THIS PAPER The two samples from 65.3 and 59.8 ft are barren of calcareous nannofossils. Two samples from 65.5 and 59.6 ft [Selected well-preserved specimens from the Millhaven core are shown in were examined by Jonathan R. Bryan of Okaloosa-Walton plate 1 as indicated below] Community College in Niceville, Fla., for their larger fora- Blackites creber (Deflandre in Deflandre and Pert, 1954) minifers, which indicate either a latest Eocene or an earliest Stradner & Edwards 1968 Oligocene age, with the Oligocene being more likely. Blackites scabrosus (Deflandre in Deflandre and Pert, 1954) Roth 1970 (this paper, pi. 1, fig. 8) Blackites spinosus (Deflandre & Pert 1954) Hay & Towe GIRARD CORE 1962 Blackites tennis (Bramlette & Sullivan 1961) Sherwood Two samples were examined from the Ellenton Forma 1974 tion in the Girard core (fig. 1) at 521.0 and 514.0 ft. Both Braarudosphaera bigelowii (Gran & Braarud 1935) Deflan samples were barren of calcareous nannofossils. dre 1947 Braarudosphaera discula Bramlette & Riedel 1954 MILLERS POND CORE Braarudosphaera stylifer Troelsen & Quadros 1971 Campylosphaera dela (Bramlette & Sullivan 1961) Hay & Three samples were examined from the Santee Lime Mohler 1967 stone in the Millers Pond core (fig. 1). Species from the Cepekiella lumina (Sullivan 1965) Bybell 1975 lowest sample at 148 ft, which contained rare calcareous Chiasmolithus bidens (Bramlette & Sullivan 1961) Hay & nannofossils with poor preservation, are as follows: Mohler 1967 Chiasmolithus consuetus (Bramlette & Sullivan 1961) Hay Braarudosphaera bigelowii (Gran & Braarud) Deflandre Helicosphaera lophota (Bramlette & Sullivan) Locker & Mohler 1967 Reticulofenestra sp. Chiasmolithus danicus (Brotzen 1959) Hay & Mohler 1967 Chiasmolithus eograndis Perch-Nielsen 1971 Species from the middle sample at 120 ft, which con Chiasmolithus expansus (Bramlette & Sullivan 1961) Hay tained frequent calcareous nannofossils with poor preserva et al. 1966 tion, are as follows: Chiasmolithus gigas (Bramlette & Sullivan 1961) Hay et al. Campylosphaera dela (Bramlette & Sullivan) Hay & 1966 Mohler Chiasmolithus grandis (Bramlette & Riedel 1954) Hay et al. Coccolithus pelagicus (Wallich) Schiller 1966 Cyclococcolithus formosus Kamptner Chiasmolithus oamaruensis (Deflandre in Deflandre and Ericsonia obruta Perch-Nielsen Pert, 1954) Hay et al. 1966 Neococcolithes sp. Chiasmolithus solitus (Bramlette & Sullivan 1961) Hay et Pemma papillatum Martini al. 1966 Pontosphaera multipora (Kamptner) Roth Chiphragmalithus acanthodes Bramlette & Sullivan 1961 Reticulofenestra daviesii (Haq) Haq Coccolithus eopelagicus (Bramlette & Riedel 1954) Bram Reticulofenestra floridana (Roth & Hay) Theodoridis lette & Sullivan 1961 Reticulofenestra umbilicus (Levin) Martini & Ritzkowski Coccolithus pelagicus (Wallich 1877) Schiller 1930 (this Rhabdosphaera sp. paper, pi. 1, figs. 1, 11) Sphenolithus moriformis (Bronnimann & Stradner) Bram Cribrocentrum reticulatum (Gartner & Smith 1967) lette & Wilcoxon Perch-Nielsen 1971 Transversopontis pulcher (Deflandre) Perch-Nielsen Cruciplacolithus primus Perch-Nielsen 1977 F12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Cruciplacolithus staurion (Bramlette & Sullivan 1961) Lithostromation operosum (Deflandre in Deflandre and Gartner 1971 Pert, 1954) Bybell 1975 Cruciplacolithus tenuis (Stradner 1961) Hay & Mohler in Lithostromation simplex (Klumpp 1953) Bybell 1975 Hay and others (1967) Lophodolithus mochlophorus Deflandre in Deflandre and Cyclagelosphaera prima (Bukry 1969) Bybell & Self-Trail Pert (1954) 1995 Lophodolithus nascens Bramlette & Sullivan 1961 Cyclococcolithus formosus Kamptner 1963 Markalius apertus Perch-Nielsen 1979 Cyclococcolithus protoannulus (Gartner 1971) Haq & Markalius inversus (Deflandre in Deflandre and Pert, 1954) Lohmann 1976 Bramlette & Martini 1964 Dictyococcites bisectus (Hay et al. 1966) Bukry & Percival Micrantholithus aequalis Sullivan 1964 1971 Micrantholithus crenulatus Bramlette & Sullivan 1961 Dictyococcites scrippsae Bukry & Percival 1971 Micrantholithus fornicatus Martini 1961 Discoaster barbadiensis Tan Sin Hok 1927 (this paper, pi. Micrantholithus pinguis Bramlette & Sullivan 1961 l,fig.2) Nannotetrina fulgens (Stradner 1960) Achuthan & Stradner Discoaster deflandrei Bramlette & Riedel 1954 (this paper, 1969 pi. 1, fig. 6) Neochiastozygus concinnus (Martini 1961) Perch-Nielsen Discoaster distinctus Martini 1958 1971 Discoaster kuepperi Stradner 1959 Neococcolithes dubius (Deflandre in Deflandre and Pert, Discoaster limbatus Bramlette & Sullivan 1961 1954) Black 1967 Discoaster lodoensis Bramlette & Riedel 1954 Neococcolithes protenus (Bramlette & Sullivan 1961) Black Discoaster mirus Deflandre in Deflandre and Pert (1954) 1967 Discoaster mohleri Bukry & Percival 1971 Pedinocyclus larvalis Bukry & Bramlette 1971 Discoaster multiradiatus Bramlette & Riedel 1954 Pemma basquense (Martini 1959) Bybell & Gartner 1972 Discoaster saipanensis Bramlette & Riedel 1954 Pemmapapillatum Martini 1959 Pemma rotundum Klumpp 1953 Discoaster sublodoensis Bramlette & Sullivan 1961 (this Pemma stradneri (Chang 1969) Perch-Nielsen 1971 paper, pi. 1, fig. 3) Placozygus sigmoides (Deflandre in Deflandre and Pert, Discoaster tanii Bramlette & Riedel 1954 1954) Black 1967 (this paper, pi. 1, fig. 9) Discoaster woodringii Bramlette & Riedel 1954 Pontosphaera multipora (Kamptner ex Deflandre 1959) Ellipsolithus distichus (Bramlette & Sullivan 1961) Sullivan Roth 1970 1964 Pontosphaera punctosa (Bramlette & Sullivan 1961) Ellipsolithus lajollaensis Bukry & Percival 1971 Perch-Nielsen 1984 Ellipsolithus macellus (Bramlette & Sullivan 1961) Sullivan Pontosphaera wechesensis (Bukry & Percival 1971) Aubry 1964 1986 Ericsonia obruta Perch-Nielsen 1971 Pseudotriquetrorhabdulus inversus (Bukry & Bramlette Ericsonia subpertusa Hay & Mohler 1967 (this paper, pi. 1, 1969) Wise in Wise and Constans (1976) fig. 10) Reticulofenestra daviesii (Haq 1968) Haq 1971 Fasciculithus tympaniformis Hay & Mohler in Hay and oth Reticulofenestra floridana (Roth & Hay in Hay and others, ers (1967) 1967) Theodoridis 1984 (this paper, pi. 1, fig. 4) Goniolithus fluckigeri Deflandre 1957 Reticulofenestra hillae Bukry & Percival 1971 Hayella situliformis Gartner 1969 Reticulofenestra umbilicus (Levin 1965) Martini & Ritz- Helicosphaera bramlettei (Miiller 1970) Jafar & Martini kowski 1968 1975 Rhabdosphaera gladius Locker 1967 Helicosphaera compacta Bramlette & Wilcoxon 1967 Rhabdosphaera inflata Bramlette & Sullivan 1961 Helicosphaera intermedia Martini 1965 Rhomboaster bramlettei (Bronnimann & Stradner 1960) Helicosphaera lophota (Bramlette & Sullivan 1961) Locker Bybell & Self-Trail 1995 1973 (this paper, pi. 1, fig. 7) Rhomboaster contortus (Stradner 1958) Bybell & Self-Trail Helicosphaera reticulata Bramlette & Wilcoxon 1967 1995 Helicosphaera seminulum Bramlette & Sullivan 1961 Rhomboaster orthostylus (Shamrai 1963) Bybell & Heliolithus cantabriae Perch-Nielsen 1971 Self-Trail 1995 Heliolithus kleinpellii Sullivan 1964 Sphenolithus anarrhopus Bukry & Bramlette 1969 Heliolithus riedelii Bramlette & Sullivan 1961 Sphenolithus capricornutus Bukry & Percival 1971 Isthmolithus recurvus Deflandre in Deflandre and Pert Sphenolithus moriformis (Bronnimann & Stradner 1960) (1954) Bramlette & Wilcoxon 1967 Lanternithus minutus Stradner 1962 Sphenolithus obtusus Bukry 1971 CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF CENOZOIC SEDIMENTS, MILLHAVEN CORE, GEORGIA F13

Sphenolithus pseudoradians Bramlette & Wilcoxon 1967 Deflandre, Georges, and Pert, Charles, 1954, Observations sur les Sphenolithus radians Deflandre in Grasse (1952) Coccolithophorides actuels et fossiles en microscopie ordi- naire et electronique: Annales de Paleontologie, v. 40, p. 115- Toweius pertusus (Sullivan 1965) Romein 1979 176. Toweius selandianus Perch-Nielsen 1979 (this paper, pi. 1, fig. 12) Edwards, L.E., Bybell, L.M., Gohn, G.S., and Frederiksen, N.O., Transversopontis fimbriatus (Bramlette & Sullivan 1961) 1997, Paleontology and physical stratigraphy of the USGS - Pregnall No. 1 core (DOR-208), Dorchester County, South Locker 1968 Carolina: U.S. Geological Survey Open-File Report 97-145, Transversopontis pulcher (Deflandre in Deflandre and Pert, 35 p. 1954) Perch-Nielsen 1967 Grasse, P.P., 1952, Traite de zoologie: Paris, Masson, 1071 p. Transversopontis pulcheroides (Sullivan 1964) Baldi-Beke 1971 (this paper, pi. 1, fig. 5) Hay, WW, Mohler, H.P., Roth, P.H., Schmidt, R.R., and Bou- Transversopontis pulchriporus (Reinhardt 1967) Sherwood dreaux, I.E., 1967, Calcareous nannoplankton zonation of the 1974 Cenozoic of the Gulf Coast and Caribbean-Antillean area and transoceanic correlation: Gulf Coast Association of Geologi Transversopontis zigzag Roth & Hay in Hay and others, cal Societies Transactions, v. 17, p. 428-480. 1967 Zygrhablithus bijugatus (Deflandre in Deflandre and Pert, Hazel, I.E., Bybell, L.M., Christopher, R.A., Frederiksen, N.O., 1954) Deflandre 1959 May, F.E., McLean, D.M., Poore, R.Z., Smith, C.C., Sohl, N.F, Valentine, P.C., and Witmer, R.J., 1977, Biostratigraphy of the deep corehole (Clubhouse Crossroads Corehole 1) near Charleston, South Carolina, chap. F of Rankin, D.W, ed., REFERENCES CITED Studies related to the Charleston, South Carolina, earthquake of 1886—A preliminary report: U.S. Geological Survey Pro Berggren, W.A., Kent, D.V., Flynn, J.J., and Van Couvering, J.A., fessional Paper 1028, p. 71-89. 1985, Cenozoic geochronology: Geological Society of Amer ica Bulletin, v. 96, p. 1407-1418. Martini, Erlend, 1971, Standard Tertiary and Quaternary calcare Berggren, W.A., Kent, D.V., Swisher, C.C., III, and Aubry, M.-P., ous nannoplankton zonation: Planktonic Conference, 2d, 1995, A revised Cenozoic geochronology and chronostratig- Rome, 1969, Proceedings, p. 739-785. raphy, in Berggren, W.A., Kent, D.V, Aubry, M.-R, and Har- Okada, Hisatake, and Bukry, David, 1980, Supplementary modifi denbol, Jan, eds., Geochronology, time scales and global cation and introduction of code numbers to the low-latitude stratigraphic correlation: SEPM (Society for Sedimentary coccolith biostratigraphic zonation (Bukry, 1973; 1975): Geology) Special Publication 54, p. 129-212. Marine Micropaleontology, v. 5, no. 3, p. 321-325. Bukry, David, 1973, Low-latitude coccolith biostratigraphic zonation, in Edgar, N.T., Saunders, J.B., Bolli, H.M., Boyce, R.E., Perch-Nielsen, Katharina, 1985, Cenozoic calcareous nannofos Broecker, W.S., Donnelly, T.W., Gieskes, J.M., Hay, W.W., sils, in Bolli, H.M., Saunders, J.B., and Perch-Nielsen, Katha Horowitz, R.M., Maurrasse, Florentin, Perez Nieto, Hernan, rina, eds., Plankton stratigraphy: New York, Cambridge Prell, Warren, Premoli Silva, Isabella, Riedel, W.R., Schnei- University Press, p. 427-554. dermann, Nahum, Waterman, L.S., Kaneps, A.G. (ed.), Her Poore, R.Z., and Bybell, L.M., 1988, Eocene to Miocene bio- ring, J.R. (ed.), Initial reports of the Deep Sea Drilling stratigraphy of New Jersey core ACGS #4—Implications for Project, v. 15: Washington, D.C., U.S. Government Printing regional stratigraphy: U.S. Geological Survey Bulletin 1829, Office, p. 685-703. 22 p., 8 fossil pis., 2 tables in pocket. ————1978, Biostratigraphy of Cenozoic marine sediments by calcareous nannofossils: Micropaleontology, v. 24, p. 44-60. Self-Trail, J.M., and Bybell, L.M., 1995, Cretaceous and Paleo- Bybell, L.M., 1982, Late Eocene to early Oligocene calcareous gene calcareous nannofossil biostratigraphy of New Jersey, in nannofossils in Alabama and Mississippi: Gulf Coast Associ Baker, J.E.B., ed., Contributions to the paleontology of New ation of Geological Societies Transactions, v. 32, p. 295-302. Jersey: Geological Association of New Jersey Contribution Bybell, L.M., and Gibson, T.G., 1985, The Eocene Tallahatta For Proceedings, v. 12, p. 102-139. mation of Alabama and Georgia—Its lithostratigraphy, bios- Wise, S.W, Jr., and Constans, R.E., 1976, Mid Eocene planktonic tratigraphy, and bearing on the age of the Claibornian Stage: correlations, northern Italy-Jamaica, W.I.: Gulf Coast Associ U.S. Geological Survey Bulletin 1615, 20 p. ation of Geological Societies Transactions, v. 26, p. 144-155.

PLATE 1 PLATE 1

[All specimens are from the Millhaven core, from Screven County, Georgia. Sample depths are given in feet below the surface. Specimen diameters are given in micrometers (jam). Designation of the calcareous nannofossil zone of Martini (1971) is shown in the upper right corner of each photomicrograph]

Figure 1. Coccosphere of Coccolithus pelagicus (Wallich) Schiller, Zone NP 14, Congaree Formation (481.5 ft) (diameter, 8.6 Jim). 2. Discoaster barbadiensis Tan Sin Hok, Zone NP 14, Congaree Formation (481.5 ft), side 1 (diameter, 13.6 jam). 3. Discoaster sublodoensis Bramlette & Sullivan, Zone NP 14, Congaree Formation (481.5 ft), side 1 (diameter, 11.0 |Ltm). 4. Reticulofenestrafloridana (Roth & Hay) Theodoridis, Zone NP 14, Congaree Formation (481.5 ft), distal view (length, 7.4 jam). 5. Transversopontis pulcheroides (Sullivan) Baldi-Beke, Zone NP 14, Congaree Formation (481.5 ft), distal view (length, 4.1 (am). 6. Discoaster deflandrei Bramlette & Riedel, Zone NP 14, Congaree Formation (481.5 ft), side 1 (diameter, 12.3 Jim). 7. Helicosphaera lophota (Bramlette & Sullivan) Locker, Zone NP 14, Congaree Formation (481.5 ft), proximal view (length, 10.6 Jim). 8. Blackites scabrosus (Deflandre) Roth, Zone NP 14, Congaree Formation (481.5 ft), distal view (diameter, 4.6 Jim). 9. Placozygus sigmoides (Deflandre) Black, Zone NP 5, Ellenton Formation (593.7 ft), proximal view (length, 7.4 Jim). 10. Ericsonia subpertusa Hay & Mohler, Zone NP 5, Ellenton Formation (593.7 ft), distal view (length, 3.7 Jim). 11. Coccolithus pelagicus (Wallich) Schiller, Zone NP 5, Ellenton Formation (593.7 ft), distal view (length, 4.8 jam). 12. Toweius selandianus Perch-Nielsen, Zone NP 5, Ellenton Formation (593.7 ft), distal view (length, 7.4 jam). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-F, PLATE 1

COCCOLITHUS, DISCOASTER, RETICULOFENESTRA, TRANSVERSOPONTIS, HELICOSPHAERA, BLACKITES, PLACOZYGUS, ERICSONIA, AND TOWEIUS

U.S. Department of the Interior U.S. Geological Survey

Dinocyst Biostratigraphy of Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia By Lucy E. Edwards

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G

Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Edited by Lucy E. Edwards

CONTENTS

Abstract ...... Gl Introduction...... 1 Previous Work...... 2 Acknowledgments ...... 2 Material and Methods ...... 2 Lithostratigraphic Framework ...... 3 Dinocysts from the Millhaven Core ...... 3 Ellenton Formation (642-570 ft) ...... 3 Snapp Formation (570-504 ft) ...... 8 Fourrm'le Branch Formation (Not Present) ...... 8 Congaree Formation (504^62 ft)...... 8 Warley Hill Formation (462^01 ft) ...... 8 Santee Limestone (401-228 ft) ...... 8 Barnwell Unit (228-0 ft)...... 8 Dinocysts from the Girard Core ...... 9 Ellenton Formation (542-481 ft) ...... 9 Snapp Formation (481^23 ft) ...... 9 Fourmile Branch Formation (423-390 ft)...... 9 Congaree Formation (390-325 ft) ...... 9 Warley Hill Formation (Not Present) ...... 9 Santee Limestone (325-250 ft) ...... 9 Barnwell Unit (250-0 ft)...... 9 Dinocysts from the Thompson Oak Core...... 12 Ellenton Formation (324-274 ft) ...... 12 Snapp Formation (Not Present)...... 12 Fourmile Branch Formation (274-251 ft)...... 12 Congaree Formation (251-182 ft) ...... 12 Warley Hill Formation (Not Present) ...... 12 Santee Limestone (182-130 ft) ...... 12 Barnwell Unit (130-0 ft)...... 12 Dinocysts from the Millers Pond Core...... 12 Ellenton Formation (284-232 ft) ...... 12 Snapp Formation (232-165 ft)...... 13 Fourmile Branch Formation (Not Present) ...... 13 Congaree Formation (165-156 ft) ...... 13 Warley Hill Formation (Not Present) ...... 14 Santee Limestone (156-82 ft) ...... 14 Barnwell Unit (82-0 ft)...... 15 Dinocysts from the McBean Core ...... 15 Ellenton Formation (305-272 ft) ...... 15 Snapp Formation (272-222 ft) ...... 15 Fourmile Branch Formation (Not Present) ...... 16 Congaree Formation (222-186 ft) ...... 16 Warley Hill Formation (Not Present) ...... 16 Santee Limestone (186-112 ft) ...... 16 Barnwell Unit (112-0 ft)...... 16 Discussion ...... 16 Taxonomic Notes ...... 17 References Cited ...... 23

m IV CONTENTS

PLATES [Plates follow References Cited]

1. Achilleodinium, Amphorosphaeridium, Areoligera, Areosphaeridium, Batiacasphaera, Carpatella, Cordosphaeridium, Cerebrocysta, Corrudinium, Cribroperidinium, and Dapsilidinium. 2. Damassadinium, Dinopterygium dadoides sensu Morgenroth (1966), Diphyes, Enneadocysta, Eocladopyxis, Fibradinium, Distatodinium, and Glaphyrocysta. 3. Hafniasphaera, Heteraulacacysta, Millioudodinium, Hystrichosphaeropsis, Homotryblium, Hystrichostrogylon, Operculodinium, and Pentadinium. 4. Pentadinium, Samlandia, Spiniferites, Systematophora, Tenua, Tectatodinium, Tuberculodinium, Turbiosphaera, and miscellaneous areoligeracean forms. 5. Andalusiella, Isabelidinium, Deflandrea, Dracodinium, Phelodinium, Charlesdowniea, Lentinia, Palaeoperidinium, Phthanoperidinium, and Selenopemphix. 6. Pseudorhombodinium, Rhombodinium, Selenopemphix, Senegalinium, Spinidinium, Wetzeliella, small peridiniacean forms, Cyclopsiella, andXenikoon.

FIGURES

1. Index map showing the Savannah River Site and locations of stratigraphic test holes in the study area ...... G2 2-6. Range and occurrence charts of dinocysts and acritarchs in the— 2. Millhaven core ...... 6 3. Girardcore...... _ 10 4. Thompson Oak core ...... 13 5. Millers Pond core ...... 14 6. McBeancore ...... 15 7. Correlation diagram by dinocyst assemblages for the five Georgia cores...... 18

TABLES

1. Samples studied by core with U.S. Geological Survey paleobotanical numbers (R numbers), depth below surface, and geologic unit...... G4 2. Slide numbers and microscope coordinates of photographed specimens...... 5 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA

Dinocyst Biostratigraphy of Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia

By Lucy E. Edwards

ABSTRACT pseudocolligerum (Stover) Bujak et al. are found in the San- tee Limestone, and Hystrichosphaeropsis Deflandre n. sp. Dinoflagellate cysts and acritarchs from five cores in A, Pentadinium Gerlach n. sp. D, and Pentadinium polypo- Burke and Screven Counties in Georgia reveal a complex dum Edwards are apparently restricted to the Santee Lime pattern of deposition and erosion. Paleocene sediments in stone. Specimens of species of the genus Wetzeliella are the Ellenton Formation include two separate assemblages. present in a few Santee samples but are not common. The older one is of early Paleocene age (Danian, Mid- Dinocyst recovery is variable in sediments of the Barn- wayan) and contains Carpatella cornuta Grigorovich; the well unit. In the Millhaven core, Batiacasphaera baculata younger assemblage contains Phelodinium sp. of Edwards Drugg, Batiacasphaera compta Drugg, and Cordosphaerid (1989, U.S. Geological Survey Professional Paper 1489-C) ium funiculatum Morgenroth indicate a late Eocene age. and is of late Paleocene age (Selandian and Thanetian, Mid- Core-to-core correlations based on the dinocyst assem wayan and Sabinian). Andalusiella sp. aff. A. polymorpha of blages show striking variations in units and thicknesses. The Edwards (1980, Geological Society of America Field Trip oldest Paleocene sediments are thickest in the updip direc Guidebooks, v. 2, p. 424-427) and Isabelidinium viborgense tion. Of the five cores studied, none contains all three of the sensu Kurita and Mclntyre (1995, Palynology, v. 19, p. 119- Fourmile Branch, Congaree, and Warley Hill Formations. 136) may be found just below and in the lower part of the Erosion by a paleo-Savannah River may have allowed selec upper assemblage. tive infilling during later transgressions and selective preser vation of the stratigraphic units. The Snapp Formation is present in varying thicknesses in four of the five cores. Rare dinocysts are present but are not age diagnostic. The Fourmile Branch Formation is early INTRODUCTION Eocene and is recognized only in the Thompson Oak core where the Snapp Formation is absent and in the Girard core. The Savannah River Site (SRS) in Aiken, Barnwell, Early Eocene dinocysts are conspicuously missing from the and Allendale Counties, S.C., has manufactured, disposed Millhaven, Millers Pond, and McBean cores. of, and stored a variety of hazardous materials since the Lower middle Eocene sediments of the Congaree For early 1950's. The U.S. Geological Survey, in cooperation mation containing Pentadinium favatum Edwards are with the U.S. Department of Energy and the Georgia Geo present in all cores. The highest occurrence of Turbio- logic Survey of the Georgia Department of Natural sphaera cf. T. galatea and the lowest occurrence of Glaphy- Resources, is conducting a study of the subsurface geology, rocysta cf. G. ? vicina may mark an important level near the hydrology, and water quality in the vicinity of the SRS. The calcareous nannofossil Zone NP 14/NP 15 boundary. Sedi goal of the study is to understand the actual and possible ments containing both P. favatum Edwards and Pentadinium future ground-water flow in the aquifers of the area. This goniferum Edwards are found only in the Millhaven core, paper focuses on the Tertiary dinocyst biostratigraphy in where they are assigned to calcareous nannofossil Zone NP Burke and Screven Counties in Georgia, directly across the 15 and to the Warley Hill Formation. Savannah River from the SRS (fig. 1). Upper middle Eocene sediments are present in the Dinoflagellates are microscopic algae with a complex Santee Limestone in all cores. The lowest occurrences of life cycle that may include an encysted stage. Chemically Cordosphaeridium cantharellus (Brosius) Gocht, Cyclop- resistant dinoflagellate cysts (dinocysts) are abundant and siella vieta Drugg & Loeblich, and Dapsilidinium well-preserved fossils in many of the Tertiary sediments in Gl G2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 30' 82 c 81° 30' SRS and surrounding areas. Clarke and others (1994, 1996) and Leeth and others (1996) described the geologic and hydrologic data from three of the cores that are used in the present study. Recent papers by Kurita and Mclntyre (1995) Aiken on the Paleocene of Manitoba, Canada, and by Edwards

33° 30' Upper Three (1996) on the Eocene of Virginia and Maryland, U.S., show Runs Creek/~ many forms similar to those encountered here.

: l / IBarnwell! Savannah \ River ACKNOWLEDGMENTS

I thank U.S. Geological Survey colleagues Joan S. 33° Allendale Baum, Laurel M. Bybell, John S. Clarke, W. Fred Falls, R. Parley Fleming, Norman O. Frederiksen, Thomas G. Gib- son, Gregory S. Gohn, and David C. Prowell, as well as Raymond A. Christopher (Clemson University), Paul F. Huddlestun (Georgia Geologic Survey, Atlanta), Joyce Lucas-Clark (Fremont, Calif.), and Robert Van Pelt (Bechtel

32° 30 Savannah River) for the generous sharing of data and ideas concerning the biostratigraphy and lithostratigraphy of the

EXPLANATION coastal plain. Paul Huddlestun provided the samples from the Thompson Oak and McBean cores. Test hole site and informal name of site

MATERIAL AND METHODS Figure 1. Index map showing the Savannah River Site and locations of stratigraphic test holes in the study area. This study is based on the dinocysts from five cores in east-central Georgia (fig. 1). They are discussed in order from most basinward (downdip) to most inshore (updip): Burke and Screven Counties in Georgia. These rapidly • The Millhaven test hole (33X048) was drilled by the evolving and distinctive fossils produce a detailed biostrati- U.S. Geological Survey in 1991-92 in northern graphic framework for the area. Two distinctive, chemically Screven County at lat 32°53'25" N., long 81°35'43" resistant microfossils of uncertain origin (acritarchs) are W. Surface elevation is 110 ft above sea level. also included in this study. • The Girard test hole (32Y020) was drilled by the U.S. Geological Survey in 1992 in southern Burke County at the lookout tower on Griffins Landing PREVIOUS WORK Road. The test hole is located 2 miles north of the town of Girard at lat 33°03'54" N., long 81°43'13" Relatively little has been published on the dinoflagel- W. Surface elevation is 250 ft above sea level. late biostratigraphy of the southeastern United States. Early • The Thompson Oak test hole (GGS-3794, TR92-6, taxonomic works by Drugg and Loeblich (1967) and Drugg Burke 12) was drilled by the Georgia Geologic Sur (1970) laid the foundation for later studies. Much of the bio- vey in 1993 in northeastern Burke County. The test stratigraphic information used for correlation with classic hole is located 21 miles south of Augusta just above Alabama localities is contained in Edwards (1977), and key the flood plain of the Savannah River at lat species were named and documented in Edwards (1982). A 33°10'42" N., long 81°47'10" W. Surface elevation is preliminary report on the biostratigraphy of the Chatta- 240 ft above sea level. hoochee area in Alabama and Georgia was given in • The Millers Pond test hole (GGS-3758, Burke 2) Edwards (1980). Prowell, Christopher, and others (1985) was drilled by the Georgia Geologic Survey in 1991 and Prowell, Edwards, and Frederiksen (1985) used in northern Burke County. The test hole is located 2 dinocysts to help correlate units in the subsurface of Geor miles west of the Savannah River and 16 miles south gia and South Carolina and to help document the ages of of Augusta, at lat 33°13'48" N., long 81°52'44" W. stratigraphic units. Firth (1987) documented the dinocyst Surface elevation is 245 ft above sea level. stratigraphy across the Cretaceous/Tertiary boundary in • The McBean test hole (GGS-3757, Burke 5) was western Georgia. drilled by the Georgia Geologic Survey in 1991 in More recently, brief papers by Edwards (1992) and northern Burke County. The test hole is located on Lucas-Clark (1992) have focused on the dinocysts of the the north shoulder of Collins Road, 1.1 miles east of DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G3

the intersection of GA 56 and Collins Road at lat downdip cores and sand with or without sandy carbonate in 33°13'38" N., long 81°55'50" W. Surface elevation is more updip cores. The Warley Hill Formation is found only 297 ft above sea level. in the Millhaven core and is primarily a carbonate sand. The Core samples were selected on the basis of favorable Santee Limestone is predominantly a carbonate that lithology and providing biostratigraphic coverage. Samples includes beds of calcareous sand and clay. The Barnwell were assigned U.S. Geological Survey paleobotanical num unit is a mixed lithologic package of sandy limestone, marl, bers by locality and letter designations by depth. Table 1 clay, and sand. The Ellenton and Snapp Formations are provides a convenient summary of these. The depth range Paleocene; the Fourmile Branch Formation, Congaree For includes the thickness of the sample as well as the uncer mation, Warley Hill Formation, Santee Limestone, and tainty of the core recovery; sample depths recorded only to Barnwell unit are Eocene (Edwards and others, this volume, the nearest foot have a least 1 ft of uncertainty in recovery. chap. B). Samples were cleaned and scraped and treated with hydrochloric and hydrofluoric acids. The samples were oxi dized using nitric acid, stained with Bismark brown, sieved DINOCYSTS FROM THE at 20 micrometers, and mounted in glycerin jelly for MILLHAVEN CORE light-microscope observation. All slides are stored at the U.S. Geological Survey, Reston, Va. Thirty-three samples were examined for dinocysts in Coordinates for dinoflagellate specimens are given for the Tertiary sediments in the Millhaven core, and all but six Olympus Vanox microscope 201526 at the U.S. Geological contained dinocysts. The occurrences of dinocyst taxa in Survey, Reston, Va. On this microscope, the coordinates for this core are shown in figure 2. the center point of a standard 25.4x76.2-millimeter slide are 27.5 and 112,7 for the vertical and horizontal axes. The ver tical coordinates increase as the stage is moved up, and the ELLENTON FORMATION (642-570 ft) horizontal coordinates increase as the slide is moved from left to right. Slide numbers and microscope coordinates of Dinocysts in the Paleocene Ellenton Formation in the photographed specimens are listed in table 2. Millhaven core were studied from eight samples from Taxonomy follows Williams and others (1998). Full 639.5-571 ft depth (table 1). The lowest sample (R4664 taxonomic citations for all forms in the text and figures are GC, at 639.5 ft) contains Areoligera volata Drugg, Carpa- found in "Taxonomic Notes." In contrast to Williams and tella cornuta Grigorovich (pi. 1, fig. 10), Spinidinium den- others (1998), however, I do not recognize the genus Tity- sispinatum Stanley, Spinidinium pulchrum (Benson) Lentin rosphaeridium Sarjeant as separate and distinct from the & Williams, and Tenua sp. cf. T. formosa of Kurita and genus Cordosphaeridium Eisenack, because both appear to Mclntyre (1995). Carpatella cornuta Grigorovich has not possess cingular processes. Except for the distinctive spe been reported from sediments younger than early Paleocene cies that are listed separately, the highly variable plexus that (Danian). Ellenton samples below 635.4 ft have been contains members of the genera Adnatosphaeridium, Areo- assigned to calcareous nannofossil Zone NP 4 (Bybell, this ligera, and Glaphyrocysta was considered to be a single tax volume, chap. F). The early-late Paleocene boundary is onomic entity (miscellaneous areoligeraceae, pi. 4, figs. 13, within Zone NP 4 (Berggren and others, 1995); the presence 14). of C. cornuta Grigorovich indicates that these sediments are from the early Paleocene part of the zone. The next higher sample (R4664 CH, at 632-632.2 ft) is LITHOSTRATIGRAPHIC FRAMEWORK dominated by small peridiniaceans such as Senegalinium microgranulatum (Stanley) Stover & Evitt and contains Details of the lithostratigraphy are given by Falls and other forms such as Palaeoperidinium pyrophorum (Ehren- Prowell (this volume, chap. A). They recognize seven Ter berg) Sarjeant and Hafniasphaera septata (Cookson & tiary units, and their terminology and correlations are fol Eisenack) Hansen, Andalusiella sp. aff. A. polymorpha of lowed here. However, the individual components of their Edwards (1980), and Deflandrea cf. D. diebelii of Drugg "Fourmile Branch/Congaree/Warley Hill unit" are discussed (1967). The remaining Ellenton samples contain similar separately. The Ellenton Formation is the lowest Tertiary assemblages that include Damassadinium californicum unit and consists of calcareous and noncalcareous sand and (Drugg) Fensome et al. (pi. 2, fig. 3), Phelodinium sp. of clay that is locally glauconitic. It is overlain by the Snapp Edwards (1989) (lowest occurrence in R4664 GD, at 620.8 Formation, a distinctive unlithified sand and overlying white ft), and Deflandrea delineata Cookson & Eisenack (lowest kaolin. The Fourmile Branch Formation is recognized only occurrence in R4664 A, at 589 ft, pi. 5, 5.5). Palaeoperidin in the Girard and Thompson Oak cores, where it consists of ium pyrophorum (Ehrenberg) Sarjeant and Fibradinium layers of clay and poorly sorted sand. The Congaree Forma annetorpense Morgenroth are present in the highest sample tion consists of interbedded sand, marl, and limestone in (R4664 D, at 571 ft). Most of the Ellenton has been G4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Table 1. Samples studied by core with U.S. Geological Survey paleobotanical numbers (R numbers), depth below surface, and geologic unit. [Fourmile, Fourmile Branch Formation; T/F, discussed in text and figures] R number Depth (ft) Unit Notes R number Depth (ft) Unit Notes Millhaven core Girard core — Continued R4664 AV __ 105 Barnwell Barren. R4705 E— — Q/JO Q/;O i Congaree T/F R4664AU— - 118 Barnwell 1 dinocyst. R4705 CF 415 Fourmile T/F R4664 AT— — 195 Barnwell 1 dinocyst. R4705AE-— 415.2^15.5 Fourmile T/F R4664 AS ----- 205 Barnwell T/F R4705D— — - 484.1^84.3 Ellenton T/F R4664AvH-UU*r ^\IVAR ———- — 210 Barnwell T/F P/C7fK f"1 514-514.3 Ellenton T/F R4664AQ— - 216.5 Barnwell T/F R4705 AD—- 517.9 518.1 Ellenton T/F R4664 AP 227.5 Barnwell T/F p/fync O 521-521.2 Ellenton T/F R4664 AO ----- 237.5 Santee Barren. R4705 A— -— 532.5-532.7 Ellenton T/F R4664 AN-— 242.5 Santee Barren. Thompson Oak core R4664 AL ----- 260 Santee Barren. P/lQ'iA P 138 Santee T/F R4664AI— — 293 Santee T/F R4836Q— -— 154 Santee T/F R4664AG— -- 313.5 Santee T/F PztS"2A P 164 Santee T/F R4664 AC ----- 346 Santee T/F R4836O— — - 172 Santee T/F R4664 Y — — 375 Santee T/F R4836N— — - 174 Santee T/F R4664X— — - 396 Santee Barren. R4836 M 181.5 Santee T/F R4664V— — - 413 Warley Hill T/F R4836 L — — - 183 Congaree T/F R4664 R — -— 442 Warley Hill T/F P/IS3A V 192 Congaree T/F R4664I.VT\J\J*T O\^/ ___—— 466 Congaree T/F R4836J— ----- 194 Congaree T/F R4664 N ___ 473.5 Congaree T/F R4836I— —— 210 Congaree T/F R4664 T -- — 483.5 Congaree T/F ~n AO^£. TLJ 231.5 Congaree T/F R4664 K — — 490 Congaree T/F T> /t oi£. r~* 245 Congaree T/F R4664 I ____ 495.5 Congaree T/F R4836 F — — - 255 Fourmile T/F R4664I\>T\JW^ JLT —____ — 498.5 Congaree T/F P/IQ1A TH 269 Fourmile T/F R4664 F -- - 527 Snapp Barren. R4836D— — - 281 Ellenton T/F R46641\>TUU*T FI..* .------_ . PzlS^A r~" ~/UH-564 ~>\J*J565 Snapp T/F 302 Ellenton T/F R4664 D - _ - 571 Ellenton T/F Millers Pond core R4664 r - _ - 577 Ellenton T/F P/ICQ1 V 72 77 Barnwell Barren. R4664 B — — - P/ICQ1 V 581 Ellenton T/F oZ— oj Santee Barren. R4664 A 589 Ellenton T/F R4581 W— — 120 Santee T/F R4664 GE — - 599.5 Ellenton T/F p/icoi \r 124 Santee T/F Iv*T\JUH-R4664 VJ-L/(TD-- ———— - 620.8 Ellenton T/F P/ICQ1 TT 148 Santee T/F R4664CH— - ^•20 ^^O 1 Ellenton T/F P/ICQ1 T 155 Santee T/F R4664 GC 639.5 Ellenton T/F P/ICQ1 C 165 Congaree T/F Girard core T5/ICQ1 p 237-242 Ellenton T/F R4705 L — — - 64.1-64.3 Barnwell Barren. P/ICQ1 O 252-257 Ellenton T/F PzL7fK V 103.6-103.8 Barnwell Barren. McBean core R4705J-— — 146.6-146.8 Barnwell T/F R4663 G— -— 181 Santee T/F

R4705 I — -— 211 1 211 3 Barnwell T/F IVH-UU^ JL ——— — 210 Congaree T/F P/CTAC TT OCT Q OCQ Santee T/F R4663 E — — - 243 Snapp No dinocysts. R4705G— — - 321.4-321.6 Santee T/F R4663 D— — - 264 Snapp T/F P/l7fK P •399 -2 399 5 Santee T/F R4663C— — - 276 Ellenton T/F R4705 AF 327.3-327.5 Consaree T/F PZL6A3 R ______9Q4 Ellenton T/F DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G5

Table 2. Slide numbers and microscope coordinates of photographed specimens. [The slide designations show the sample number (table 1) followed by the slide number in parentheses. Coordinates are given for Olympus Vanox micro scope 201526 at the U.S. Geological Survey, Reston, Va.] Figure Slide Coordinates Figure Slide Coordinates Plate 1 Plate 4 TO 3s/7f: c 1 ______R4664 K (1) 31.1x83.0 1 ...... R4664 AI (4) JJ. JA/U.J 2——— ______R4664 O (3) 20.2x93.2 2 ______— ___..__ R4664 AI (4) Zl-H-A/H-.O91 4x74 R 3— ______R4705 E (2) 33.5x74.5 3 . — -__——.—-. P/IC16 \f l^i\ 28.4x97.0 4 ______R4705 D (2) 18.7x80.3 4 .——..——.—— R4664 AC (3) 31.4x103.8 5 ______R4581 Q (4) 22.6x81.2 5 ...... R4664 AC (3) 24 ^3x72 3 6—— ______.. R4664 R (4) 27.6x98.4 6 ______R4705 I (3) 24 0x75 3 7 ______R4664AS(1) 30.7x86.0 7 ______R4705 AD (2) 33.7x76.4 8,9————— R4664 AS (1) 30.2x81.4 R4705 G (3) 24.9x90.4 10 —— — ——— R4664 GC (1) 20.4x97.0 Q R4664 AR (1) j35 7x1 04 9 11 ______R4664 AS (1) 33.7x78.6 10,11————— R4705 AD (2) 33.6x76.3 12 13 ____ - R4664 K (1) 28.2x79.1 12—————— R4664K(1) 30.3x78.0 14 ______R4664 AC (3) 29.8x81.4 1 3 ______R4664 K (1) 'ji Qv87 1 15 ______R4705 I (3) 35.6x90.6 14...... — ...... TJ/ICO 1 T> / A\ T.f. 1vQ1 1 16 —— —— ——— R4664 O (3) 34.3x89.4 Plate 5 17 ______R4664 AC (3) 27.3x103.4 1 .—...————— P.45R1 R (1 ^ 23.2x74.6 1 8 R4705 I (3) 26.9x94.4 2 ——————— R4663 C (4) Ol 1 vQ^ ^ Plate 2 3 ______TJ/ICS1 T> /I \ 26.0x73.0 1,2—————— R4663 B (4) 34.5x93.8 4 ______R4836 D (3) 99 4v7S 9 3— ______R4664 A (3) 22.1x71.8 5 ______R4664 A (3) 93 5x997 3 4 ______R4664 AS (1) 30.9x86.7 6 ______— - R4705 AD (2) 27' ••2x95i-'A;7j.J 5 5 ______R4664 O (3) 19.4x103.8 7 ...... P. 4705 PF ("[ ^ ^9 6x79 4 6— ______... R4664 AQ (2) 37.5x80.7 R4705 30.5x107.9 7 ______R4705 E (2) 21.1x75.0 9 ______R4664 AS 24.6x78.8 R4664 A (3) 19.4x97.7 10—————— R4836 D (3) 18.2x74.6 9 ______R4664AR(1) 37.2x84.5 1 1 ______R4664 AQ (2) 37.4x98.2 10 12————— R4664 O (3) 34.3x76.4 12—————— R4705 F (Y\ 1 7 9x80 4 13 ______R4705 E (2) 30.4x75.6 13—...————. 23 7x82 8 14 ______R4836 K (3) 26.0x71.1 it R4663 C (4) 33 4x95 2 15 ._...... ______R4705G(3) 30.4x89.0 15 ______R4664 AQ (2) •^^9 ^xRfiAOO. J3 Plate 3 16, 17 — — — — R4664 O (3) 26.0x95.7 1 ______R4836 F (2) 30.0x76.0 1 8 R4664 V (4) 1 O Qs^Q 1 A 2 3 - ___ _ . R4836 R (3) 22.6x79.6 Plate 6 4 R4663 G (3) 33.2x94.2 1 ...... P4705 F Cy\ 29.8x95.6 5 ...... R4663 G (3) 21.9x77.1 2 —————— R4664 AC (4-) 34.6x69.6 6— — — ______— R4664 AC (3) 34.7x84.7 3 ...... _...... _ R4705 I (3) ^ / 7 9...... R4836 R (3) 17.8x75.3 4 ______R4664 V (4) 1 8 3x78' 9 10 — — - — — — R4705 AD (2) 26.9x101.6 5 ______P/l<81 P ^1 "\ 98 8^1 C\A 8 11 ————...... R4836 E (3) 19.2x89.6 6, 10————— R4836 C (3) 32.4x80.8 12 —————.— R4705 I (3) 28.9x86.7 7 ______R4664K(1) ^c 1 vQ1 8 13 ...... R4836 N (4) 35.0x107.8 R4705 B (3) 28.9x94.8 14 ______R4664 O (3) 34.8x85.1 Q R4664 AQ (2) 22.0x74.4 15 ______R4664 N (2) 30.8x86.6 11-———————————— R4664 L (1) 26 9x83 5 16 ______R4664 AC (3) 35.7x71.7 12——————— R4581 V (4) 18.3x79.0 17 —...... -..... R4664 AR (1) 36.5x101.9 13 ______R4664 D (4) 1 8 R4664 AR (1) 26.4x94.9 14——————— R4664 F (4} 1 Q Q\x'7O 1 1Q 91 -__-_._. P48^pm 94 1 vir»8 n 15 ______R4663 C (4) 31.4x91.4 \f\ O A ^Q 1 1? f 1 \ 99 7x73' 5 17——————— R4664 AS (1) 25 3x86 8 18. ______— P4664 r» (A.\ 9Q 0x81 0 G6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

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Figure 2. Range and occurrence chart of dinocysts and acritarchs in the Millhaven core. Lithostratigraphy from Falls and Prowell (this volume, chap. A). R=reworked; cf=compares with; ?=questionably identified; l=single specimen. a § DEPTH, IN FEET

FORMATIO 0 LITHOSTRATIGRAPHIC UNIT n 5 F * o O5 n rn-< on 5' 11 H W II I SAMPLES OF THE R4664 SERIES t—I > O m O I o oo (TABLE 1) on o :co H _j =; =; »j tj "J y; J^3 3 § I § § |> ———•——————————•—•——————•—• ------Lingulodinium machaerophorum K •^——————————————————————•-«•• ------Samlandia chlamydophora ^3 -•——•————————————•——————< ------...... Diphyes ficusoides 2 ------...... - Eocladopyxis n. sp. A * ------Glaphyrocysta cf.G.? vicina ^ ------Melitasphaeridium pseudorecurvatum O ———•————————————• ------...... _ . . . _ Corrudinium sp. I of Edwards (1984) , ———————————————————————•------Phthanoperidinium echinatum g ——————————•—————————————•-• ------Dinopterygium cladoides sensu Morgenroth (1966) J*3 •——•------. . . . .-.._.-....-..---.. Operculodinium spp. H •—————————————•—• ------Areosphaeridium diktyoplokus > •———————————————• ------Lentinia serrata ?$ •——•———•——•——•—• ------Pentadinium goniferum ^ •——•——————•—————•——————•-• ------Hystrichokolpoma rigaudiae & - - •------. - . . - . . . . Muratodinium fimbriatum S - - - •------...... Selenopemphix sp. M - - - •—————————•------....-- Charlesdowniea coleothypta S ------a ------Millioudodinium sp. I of Edwards (1984) H ------*——•—• ------Pentadinium polypodum ^ •—————•————————•------Cordosphaeridium cantharellus on •—————•———————••------Distatodinium ellipticum >-r\ •————•——————• ••------Enneadocysta spp. 2 ------Samlandia chlamydophora sensu Stover and Hardenbol (1993) 2 ------Rhombodinium draco ^ •—•——————< ••• ------Phthanoperidinium comatum 3 ------Cribroperidinium tenuispinosum •<, ------Pentadinium membranaceum M -•-*•------Lejeunecysta spp. H -————————• ------Cyclopsiella vieta O ------•-••------Pentadinium laticinctum (verm.) S ------«—• ------Batiacasphaera baculata on ------> MJ ------Charlesdowniea variabilis (sensu amplo) ".~ ------•-••• ------Pentadinium laticinctum laticinctum ^ ------o ------Batiacasphaera compta Q ------•»------Spinidinium spp. & ------*------Tuberculodinium n. sp. A O ------«•------Cordosphaeridium funiculatum >• ------0 ------Corrudinium incompositum ------9 ------Deflandreaphosphoritica

o G8 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA assigned to the early late Paleocene calcareous nannofossil to NP 15 in the Millhaven core. The dinocyst assemblages Zone NP 5, but the uppermost part of the Ellenton (above in these samples correspond to those reported in part of the 578 ft) has been placed in the middle late Paleocene Zone unit E4 of Prowell, Christopher, and others (1985). NP 8 (Bybell, this volume, chap. F).

SANTEE LIMESTONE (401-228 ft) SNAPP FORMATION (570-504 ft) Eight samples were examined for dinocysts within the A single sample in the Snapp Formation (R4664 E, at Santee Limestone; four of these are barren. One sample 564-565 ft) produced rare, small peridiniacean dinocysts (R4664 Y, at 375 ft) contained only two specimens, both of (pi. 6, fig. 14), as well as miscellaneous areoligeracean Pentadinium goniferum Edwards. The three remaining sam forms and Cordosphaeridium Eisenack sp. This Snapp For ples (R4664 AC, at 346 ft; R4664 AG, at 313.5 ft; and mation sample remains undated paleontologically. In this R4664 AI, at 293 ft) produced well-preserved, diverse sample, the Snapp is at least marginally marine, unless all dinocysts that include Cordosphaeridium cantharellus (Bro- specimens are reworked. A higher sample (R4664 F, at 527 sius) Gocht (pi. 1, fig. 14), Distatodinium ellipticum (Cook- ft) did not contain dinocysts. son) Eaton, P. goniferum Edwards (pi. 3, fig. 16), Pentadinium polypodum Edwards (pi. 4, fig. 2), Rhombod- inium draco Gocht (pi. 6, fig. 2), Samlandia chlamydophora FOURMILE BRANCH FORMATION Eisenack sensu Stover and Hardenbol (1993) (pi. 4, fig. 4), (NOT PRESENT) and Areosphaeridium diktyoplokum (Klumpp) Eaton. This assemblage is typical of the late middle Eocene and sug The Fourmile Branch Formation is not present in the gests correlation with the upper part of the Lisbon Forma Millhaven core. Sediments containing marine middle tion or the Gosport Sand in Alabama. Three samples higher Eocene dinocysts directly overlie the Snapp Formation. in the Santee (R4664 AL, at 260 ft; R4664 AN, at 242.5 ft; and R4664 AO, at 237.5 ft), as well as one near its base CONGAREE FORMATION (504-462 ft) (R4664 X, at 396 ft), are barren. Santee sediments above 368 ft in the Millhaven core have been assigned to late mid The dinocyst assemblages in six samples in the Conga- dle Eocene calcareous nannofossil Zone NP 17 (Bybell, this ree Formation from 498.5-466 ft were studied. All contain volume, chap. F). Pentadinum favatum Edwards (pi. 3, fig. 15). The lower five samples (R46641, J, K, L, and N) contain Turbiosphaera cf. T. galatea (pi. 4, fig. 12), which is reported from the upper BARNWELL UNIT (228-0 ft) part of the Tallahatta Formation in Alabama (Edwards, Seven samples from the Barnwell unit were examined 1977) and unit E3 of Prowell, Christopher, and others for dinocysts; four were productive, and three are barren or (1985). The absence of Hafniasphaera goodmanii Edwards contain only a single specimen. suggests that these samples are of middle Eocene age, rather than early Eocene age, and that lower Eocene sediments are Samples from the Barnwell unit are above the highest not present in this core. The calcareous nannofossils in these appearance of P. goniferum Edwards and are most likely of lower samples are assigned to Zone NP 14 (Bybell, this vol late Eocene age. The basal Barnwell sample (R4664 AP, at ume, chap. F). 227.5 ft) contains the lowest occurrence of Charlesdowniea variabilis (Bujak) Lentin & Vozzhennikova and Batiaca- The assemblage at 466 ft (R4664 O) contains the low est occurrence Glaphyrocysta cf. G.I vicina (pi. 2, figs. 10- sphaera baculata Drugg (pi. 1, fig. 7). Higher samples (R4664 AR, at 210 ft, and R4664 AS, at 205 ft) contain B. 12) and appears to be correlative with the lowest part of the Lisbon Formation in Alabama (Edwards, unpub. data). This baculata Drugg or Batiacasphaera compta Drugg (pi. 1, figs. 8-9) or both, which suggest correlation with the upper level could be assigned to either calcareous nannofossil Eocene Yazoo Clay in Alabama, and Cordosphaeridium Zone NP 14 or NP 15 (Bybell, this volume, chap. F). funiculatum Morgenroth (pi. 1, fig. 11), which is found in the Gosport Sand and Moodys Branch Formation (upper WARLEY HILL FORMATION (462-401 ft) middle Eocene) in Alabama and the Parkers Ferry and Harleyville Formations (lower part of the Cooper Group, Both Pentadinium favatum Edwards and Pentadinium upper Eocene) in South Carolina (Edwards, 1977; unpub. goniferum Edwards are present in the samples of the Warley data). Three samples above 205 ft are barren or nearly so Hill Formation at 442 and 413 ft (R4664 R and V). These (R4664 AT, AU, AV, at 195, 118 and 105 ft, respectively). species overlap in a thin interval within the lower, but not Barnwell sediments in the Millhaven core have been lowest, part of the Lisbon Formation in Alabama, which has assigned to calcareous nannofossil Zones NP 17 and 19/20- been dated as NP 15 or NP 16 (Wrenn, 1996). It is assigned 21(?) (Bybell, this volume, chap. F). DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G9

~~DINOCYSTS FROM THE GIRARD CORE CONGAREE FORMATION (390-325 ft)~~

Two samples were studied within the Congaree Forma Sixteen samples were taken for dinocysts in the Ter tion. The lower sample (R4705 E, at 362-362.3 ft) contains tiary sediments from the Girard core and all but two con a variety of middle Eocene dinocysts that suggest correla tained dinocysts. The occurrences of dinocyst taxa in this tion with the lower part of the Lisbon Formation in Ala core are shown in figure 3. bama. Important species include Pentadinium favatum Edwards, Corrudinium sp. I of Edwards (1984), Phthanope- ridinium echinatum Eaton, Pseudorhombodinium lisbon- ELLENTON FORMATION (542-481 ft) ense Wrenn (pi. 6, fig. 1), Samlandia chlamydophora Eisenack, Wetzeliella articulata Eisenack, Glaphyrocysta cf. Dinocysts in the Paleocene Ellenton Formation in the G.I vicina (pi. 2, fig. 13), and Eocladopyxis Morgenroth n. Girard core were studied from five samples from 532.7 to sp. A (pi. 2, fig. 7). The higher Congaree sample (R4705 484.1 ft. As in the Millhaven core, both early Paleocene and AF, at 327.3-327.5 ft) contains a similar dinocyst assem late Paleocene assemblages were recorded. blage. The lowest sample (R4705 A, at 532.5-532.7 ft) con tains a nondiagnostic dinoflora consisting of small peridini- WARLEY HILL FORMATION (NOT PRESENT) acean cysts, Spiniferites Mantell spp., and a few specimens of the areoligeracean group. The next higher samples No samples containing both P. favatum Edwards and P. (R4705 B, at 521.0-521.2 and R4705 AD, at 517.9-518.1) goniferum Edwards were found. Sediments correlative with contain early Paleocene (Danian, Midwayan) dinocysts, the Warley Hill in the Millhaven core apparently are not including Carpatella cornuta Grigorovich, Tenua sp. cf. T. present in the Girard core. formosa of Kurita and Mclntyre (1995) (pi. 4, fig. 7), Tecta- todinium rugulatum (Hansen) McMinn (pi. 4, figs. 10, 11) and Deflandrea n. sp. aff. D. truncata Stover (pi. 5, fig. 8). SANTEE LIMESTONE (325-250 ft) This assemblage is also dominated by small peridiniacean cysts. The sample R4705 C (at 514.0-514.3 ft) contains a Three samples were examined from the Santee Lime stone in the Girard core. The lowest Santee sample (R4705 rather sparse dinoflora that includes a fragment question F, at 322.3-322.5 ft) contains a very sparse and relatively ably identified as C. cornuta Grigorovich. The sample nondiagnostic dinocyst assemblage. It does, however, con R4705 D (at 484.1-484.3 ft) contains a typical late Pale tain the middle Eocene species Pentadinium goniferum ocene (Selandian, late Midwayan) dinoflora, which is also Edwards. The sample a foot higher (R4705 G, at 321.4- dominated by small peridiniacean cysts and contains Dam- 321.6 ft) contains the lowest occurrence of Cordosphaerid- assadinium californicum (Drugg) Fensome et al. and Phelo- ium cantharellus (Brosius) Gocht. The sample at 257.8-258 dinium sp. of Edwards (1989). ft (R4705 H) contains a well-preserved, diverse dinocyst assemblage that includes Pentadinium polypodum Edwards, Samlandia chlamydophora Eisenack sensu Stover and SNAPP FORMATION (481-423 ft) Hardenbol (1993), and Enneadocysta spp. These and other species present are characteristic of upper middle Eocene No samples were taken from the sand and clay of the sediments correlative with the upper Lisbon Formation and Snapp Formation in the Girard core. the Gosport Sand (Edwards, 1977; unpub. data) and with unit E5 of Prowell, Christopher, and others (1985).

~~FOURMILE BRANCH FORMATION (423-390 ft) BARNWELL UNIT (250-0 ft)~~

Two samples were studied within the Fourmile Branch Four samples from the Barn well unit were studied Formation. The age of these samples is Eocene. However, from the Girard core. Sample R4705 I (at 211.1-211.3 ft) attempts to determine whether they are early or middle contains the species Rhombodinium perforatum (Jan du Eocene were inconclusive. In the lower sample (R4705 AE, Chene & Chateauneuf) Lentin & Williams (pi. 6, fig. 3), at 415.2-415.5 ft), Homotryblium tenuispinosum Davey & Charlesdowniea variabilis (Bujak) Lentin & Vozzhenni- Williams is tentatively identified. A nearby repeat sample kova, and Corrudinium incompositum (Drugg) Stover & (R4705 CF, at 415 ft) recovered a single specimen of Dra Evitt (pi. 1, fig. 15). These species suggest a late middle or co dinium varielongitudum (Williams & Downie) Costa & late Eocene age. The sample R4705 J (at 146.6-146.8 ft) Downie (pi. 5, fig. 7). contains a very sparse and nondiagnostic dinocyst G10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

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Figure 3. Range and occurrence chart of dinocysts and acritarchs in the Girard core. Lithostratigraphy from Falls and Prowell (this volume, chap. A). cf=compares with; ?=questionably identified. DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA Gil

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Figure 3. Continued. G12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA assemblage. Samples R4705 K and L (at 103.6-103.8 and with the upper part of the Tallahatta Formation and the 64.1-64.3 ft) are barren of dinocysts. lower part of the Lisbon Formation in Alabama. Sample R4836 H (at 231.5 ft) is more likely correlative with the upper part of the Tallahatta because it contains Turbio- DINOCYSTS FROM THE sphaera cf. T. galatea. The three samples from 194-183 ft THOMPSON OAK CORE (R4836 J, K, and L) are more likely correlative with the lower part of the Lisbon because they contain Glaphyro- Sixteen samples were taken for dinocysts in the Ter cysta cf. G.? vicina (pi. 2, fig. 14). Sample R4836 I (at 210 tiary sediments of the Thompson Oak core, and all con ft) does not contain sufficient diagnostic taxa. tained dinocysts. The occurrences of dinocyst taxa in the Thompson Oak core are shown in figure 4. WARLEY HILL FORMATION (NOT PRESENT)

ELLENTON FORMATION (324-274 ft) The Warley Hill Formation is not present in the Thompson Oak core. Dinocysts in the Ellenton from the Thompson Oak core were studied from two samples. Both are Paleocene (Danian or Selandian, Midwayan). The lower sample SANTEE LIMESTONE (182-130 ft) (R4836 C, at 302 ft) is dominated by Areoligera volata Drugg and small peridiniaceans. Important species present Six samples of the Santee Limestone were studied include Tectatodinium rugulatum (Hansen) McMinn, Dam- from the Thompson Oak core. The five samples from assadinium californicum (Drugg) Fensome et al., Tenua sp. 181.5-154 ft depth contain a distinctive dinocyst assem cf. T. formosa of Kurita and Mclntyre (1995), and Deflan- blage that includes Pentadinum goniferum Edwards, Penta- drea n. sp. aff. D. truncata Stover. The sample lacks Carpa- diniurn Gerlach n. sp. D (pi. 3, figs. 19-21), Enneadocysta tella cornuta Grigorovich but contains other species Stover & Williams spp., Heteraulacacysta porosa Bujak, recorded in the early Paleocene samples from the Mill- and Hystrichostrogylon membmniphorum Agelopoulos (pi. haven, Girard, and Millers Pond cores. The upper sample 3, fig. 13). These forms indicate an age in the later part of (R4836 D, at 281 ft) is dominated by small peridiniaceans the middle Eocene and correlation with the upper part of the and contains Andalusiella sp. aff. A. polymorpha of Lisbon Formation, the Gosport Sand, or the Moodys Branch Edwards (1980) (pi. 5, fig. 4) and Phelodinium sp. of Formation in the Gulf Coast. The highest Santee Limestone Edwards (1989). It is of late Paleocene age (Selandian). sample (R4836 R, at 138 ft) contains the lowest occurrence of Cordosphaeridium cantharellus (Brosius) Gocht.

SNAPP FORMATION (NOT PRESENT) BARNWELL UNIT (130-0 ft) The Snapp Formation is not present in the Thompson Oak core. Sediments containing marine Eocene dinocysts Sediments of the Barn well unit in the Thompson Oak directly overlie marine Paleocene sediments. core were not sampled in this study.

FOURMILE BRANCH FORMATION (274-251 ft) DINOCYSTS FROM THE MILLERS POND CORE Two samples from 269 and 245 ft contain early Eocene dinocysts, including Hafniasphaera goodmanii Edwards Nine samples were taken in Tertiary sediments of the (pi. 3, fig. 1), primitive forms of Pentadinium favatum Millers Pond core; seven contained dinocysts, and the Edwards, and Wetzeliella articulata Eisenack. The lowest of uppermost two samples are barren. The occurrences of these contains Homotryblium abbreviation Eaton (pi. 3, fig. dinocyst taxa in this core are shown in figure 5. 11). These assemblages are likely to be of early Eocene age.

ELLENTON FORMATION (284-232 ft) CONGAREE FORMATION (251-182 ft) Dinocysts in the Ellenton Formation from the Millers Six samples in the Congaree from the Thompson Oak Pond core were studied from two samples (R4581 Q, at core were studied for dinocysts. The lowest sample (R4836 252-257 ft; R4581 R, at 237-242 ft). Both contain dinocyst G from 245 ft) contains the highest occurrence of Hafnia assemblages of Paleocene age (Danian or Selandian, Mid sphaera goodmanii Edwards. Five samples from 231.5- wayan). The lower sample contains Areoligera volata 183.5 ft all contain dinofloras that are roughly correlative Drugg (pi. 1, fig. 5), Carpatella cornuta Grigorovich, Spini- DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G13

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~~Figure 4. Range and occurrence chart of dinocysts and acritarchs in the Thompson Oak core. Lithostratigraphy from Falls and Prowell (this volume, chap. A). ?=questionably identified.~~

dinium densispinatum Stanley, Spinidinium pulchrum (Ben- SNAPP FORMATION (232-165 ft) son) Lentin & Williams, Tectatodinium rugulatum (Hansen) McMinn, and Tenua sp. cf. T. formosa of Kurita and Mcln The interval from 232 to 165 ft in the core consisted of coarse sand and thoroughly oxidized kaolinitic clay and was tyre (1995). C. cornuta has not been reported from sedi not sampled for dinocysts. ments younger than early Paleocene. This sample contains early Paleocene pollen (Frederiksen, this volume, chap. H). The upper sample in the Ellenton contains a distinctive FOURMILE BRANCH FORMATION assemblage including Andalusiella sp. aff. A. polymorpha (NOT PRESENT) of Edwards (1980) (pi. 5, fig. 3), Deflandrea cf. D. diebelii The Fourmile Branch Formation is not present in the of Drugg (1967), Senegalinium microgranulatum (Stanley) Millers Pond core. There is no evidence of early Eocene Stover & Evitt (pi. 6, fig. 5), Isabelidinium viborgense sensu marine deposition in this core. Kurita and Mclntyre (1995), and Damassadinium californicum (Drugg) Fensome et al. The species in this upper sam ple were reported together in the Porters Creek Clay in CONGAREE FORMATION (165-156 ft) Alabama (Edwards, 1980). However, the assemblage could Directly above the oxidized clays of the Snapp Forma perhaps range into slightly younger sediments, because the tion is a 9-ft-thick unit of silty sand. A sample just above the Naheola Formation was not included in the 1980 study. base (R4581 S, at 165 ft) contains a dinocyst assemblage Kurita and Mclntyre (1995) used the lowest occurrence of/. that includes Diphyes colligerum (Deflandre & Cookson) viborgense Heilmann-Clausen to mark the base of the Cookson, Phthanoperidinium echinatum Eaton, Polysphaer- Selandian (earliest late Paleocene) in Manitoba, Canada. idium zoharyi (Rossignol) Bujak et al., somewhat primitive G14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

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Figure 5. Range and occurrence chart of dinocysts and acritarchs in the Millers Pond core. Lithostratigraphy from Falls and Pro well (this volume, chap. A). R=reworked; cf=compares with; ?=questionably identified. forms of Pentadinium favatum Edwards, Turbiosphaera cf. This assemblage could represent the interval of overlap of T. galatea, and Wetzeliella articulata Eisenack. This assem the ranges of P. favatum Edwards and P. goniferum blage correlates with that recorded from the upper part of Edwards, or it could represent a lag deposit at the base of the Tallahatta Formation in Alabama, which is in the lower the overlying unit. Because P. favatum Edwards and Turbio part of the middle Eocene. sphaera cf. T. galatea are each represented by one poorly preserved specimen, and because Turbiosphaera cf. T. galatea and P. goniferum Edwards do not overlap in other WARLEY HILL FORMATION (NOT PRESENT) cores, the interpretation of this sample as a lag deposit The Warley Hill Formation is not present in the Millers appears more likely. Pond core. Three samples (R4581 U, V, W, at 148, 124, and 120 ft) contain diverse and abundant dinocyst assemblages including Pentadinium goniferum Edwards, Pentadinium SANTEE LIMESTONE (156-82 ft) Gerlach n. sp. D, Samlandia chlamydophora Eisenack, Five samples from the Santee Limestone were studied Hystrichostrogylon coninckii Heilmann-Clausen, Cordo- from the Millers Pond core. The lowest sample (R4581 T, at sphaeridium cantharellus (Brosius) Gocht, and 155 ft) contains a diverse dinocyst assemblage including Dapsilidinium pseudocolligerum (Stover) Bujak et al. This Achilleodinium biformoides (Eisenack) Eaton and Pentadin is a late middle Eocene assemblage, correlative with the ium goniferum Edwards, and single specimens of Pentadin upper part of the Lisbon Formation, Gosport Sand, or ium favatum Edwards and Turbiosphaera cf. T. galatea. Moodys Branch Formation in Alabama. The uppermost DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G15

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~~o • M O 200 - CONGAREE T : FM. - F O O 0 0 O • "~~

SNAPP - E No Dinocysts \ '< FM. - D O p ELLENTON \s — B ' 300 - FORMATION ••••Inl O O Figure 6. Range and occurrence chart of dinocysts and acritarchs in the McBean core. Lithostratigraphy from Falls and Prowell (this volume, chap. A). ?=questionably identified. sample in the Santee Limestone (R4581 X, at 82-83 ft) is wayan) dinocyst assemblages. The lower sample (R4663 B, barren of dinocysts. at 294 ft) includes Damassadinium californicum (Drugg) Fensome et al. (pi. 2, figs. 1-2), Palaeoperidinium pyropho rum (Ehrenberg) Sarjeant, and Tectatodinium rugulatum BARNWELL UNIT (82-0 ft) (Hansen) McMinn. The upper sample (R4663 C, at 276 ft) includes Andalusiella sp. aff A. polymorpha of Edwards Barnwell unit sediments were examined for dinocysts in a single sample at 72-77 ft in the Millers Pond core. The (1980), Deflandrea cf. D. diebelii of Drugg (1967), sample proved barren. Hafniasphaera septata (Cookson & Eisenack) Hansen, Isa- belidinium viborgense sensu Kurita and Mclntyre (1995) (pi. 5, fig. 2), and P. pyrophorum (Ehrenberg) Sarjeant. The DINOCYSTS FROM THE MCBEAN CORE lower sample is likely to be early Paleocene, as indicated by the presence of T. rugulatum (Hansen) McMinn. The upper Six samples were taken in Tertiary sediments of the sample is late Paleocene (Selandian, Midwayan) because of McBean core; five contained dinocysts and one yielded only the presence of /. viborgense sensu Kurita and Mclntyre pollen. The occurrences of dinocyst taxa in this core are (1995). shown in figure 6.

~~SNAPP FORMATION (272-222 ft) ELLENTON FORMATION (305-272 ft)~~

Two samples from the Ellenton Formation in the A single fragmental specimen of the areoligeraceae McBean core yielded Paleocene (Danian or Selandian, Mid- jroup was recovered from the sample of the Snapp Forma- G16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA tion at 264 ft (R4663 D) in the McBean core. A second sam pyrophorum (Ehrenberg) Sarjeant, and Deflandrea cf. D. ple (R4663 E, at 243 ft) yielded no dinocysts. diebelii of Drugg (1967) (pi. 5, fig. 6) and may be domi nated by small peridiniaceans (pi. 6, figs. 13, 15, 16). Andalusiella sp. aff. A. polymorpha of Edwards (1980) and FOURMILE BRANCH FORMATION Isabelidinium viborgense sensu Kurita and Mclntyre (1995) (NOT PRESENT) may be found just below, and in the lower part of, the upper assemblage. Kurita and Mclntyre (1995) used the lowest The Fourmile Branch Formation is not recognized in occurrence of I. viborgense Heilmann-Clausen to approxi the McBean core. mate the early-late Paleocene (Danian-Selandian) boundary in Manitoba, Canada. In the Millhaven core, the uppermost CONGAREE FORMATION (222-186 ft) Ellenton sample has been placed in calcareous nannofossil Zone NP 8 (Bybell, this volume, chap. F) although the A single sample of the Congaree Formation in the dinocyst assemblage is not noticeably different from assem McBean core (R4663 F, at 210 ft) contains the early middle blages in the samples below it. Eocene species Eocladopyxis Morgenroth n. sp. A and Pen- The Snapp Formation is present in varying thicknesses to, dinium favatum Edwards, and long-ranging species. in four of the five cores. It is conspicuously absent in the Thompson Oak core, and an upper kaolinitic part is not present in the McBean core. Because the Snapp Formation WARLEY HILL FORMATION (NOT PRESENT) is present in the most updip cores, it was probably also The Warley Hill Formation is not recognized in the present in the Thompson Oak area originally but subse McBean core. quently removed. Marginal marine or marine dinocysts are found in two samples of the lower part of the Snapp Forma tion in the Millhaven and McBean cores. However, the SANTEE LIMESTONE (186-112 ft) assemblages are not age diagnostic and could perhaps be reworked from the Ellenton. A single sample of the Santee Limestone in the Lower Eocene sediments are identified in the Fourmile McBean core (R4663 G, at 181 ft) yielded a diverse middle Branch Formation in the Thompson Oak core on the basis of Eocene dinocyst assemblage. Heteraulacacysta porosa Hafniasphaera goodmanii Edwards and primitive forms of Bujak, Heteraulacacyata pustulosa Jan du Chene & Adedi- Pentadinium favatum Edwards. Homotryblium abbreviatum ran (pi. 3, fig. 5), Pentadinium goniferum Edwards, and Eaton is also present. Sediments in the Fourmile Branch in Samlandia chlamydophora Eisenack are present The the Girard core contain Dracodinium varielongitudum (Wil assemblage resembles that in the Santee Limestone in the liams & Downie) Costa & Downie and Homotryblium Thompson Oak core. tenuispinosum Davey & Williams and may be of early Eocene age. Early Eocene dinocysts are conspicuously missing from the Millhaven, Millers Pond, and McBean BARNWELL UNIT (112-0 ft) cores. Sediments of the Barnwell unit from the McBean core Middle Eocene Congaree sediments correlative with were not sampled in this study. the uppermost part of the Tallahatta Formation and the lower part of the Lisbon Formation are present in all cores. Samples contain diverse dinocyst assemblages, which DISCUSSION include Achilleodinium biformoides (Eisenack) Eaton (pi. 1, figs. 1-3), Diphyes colligerum (Deflandre & Cookson) Paleocene sediments in the cores studied include two Cookson, Eocladopyxis Morgenroth n. sp. A, Glaphyrocysta separate assemblages. The older one is early Paleocene cf. G.I vicina, Phthanoperidinium echinatum Eaton (pi. 5, (Danian, Midwayan) and contains Carpatella cornuta Grig- figs. 16, 17), Pentadinium favatum Edwards, Samlandia orovich, Spinidinium pulchrum (Benson) Lentin & Williams chlamydophora Eisenack (pi. 4, fig. 3), Turbiosphaera cf. T. (pi. 6, figs. 6, 10), Tectatodinium rugulatum (Hansen) galatea, Wetzeliella articulata Eisenack (pi. 6, figs. 7, 11), McMinn, and Tenua sp. cf. T. formosa of Kurita and Mcln- and many areoligeracean forms. The highest occurrence of tyre (1995). This assemblage is assigned to calcareous nan- Turbiosphaera cf. T. galatea and the lowest occurrence of nofossil Zone NP 4 in the Millhaven core. The younger Glaphyrocysta cf. G. ? vicina may mark an important level, assemblage contains Phelodinium sp. of Edwards (1989) correlative with the Tallahatta Formation-Lisbon Formation (pi. 5, fig. 10) and is assigned to calcareous nannofossil boundary in Alabama and the E3-E4 boundary (of Pro well, Zones NP 5 and NP 8 in the Millhaven core (Bybell, this Christopher, and others, 1985) in Georgia. Calcareous nan- volume, chap. F). Both assemblages contain Damassadin- nofossils in the Millhaven core indicate that this boundary is ium californicum (Drugg) Fensome et al., Palaeoperidinium near the NP 14/NP 15 boundary. DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G17

Sediments containing both Pentadinium favatum absence of the Snapp corresponds with the presence of the Edwards and Pentadinium goniferum Edwards are found Fourmile Branch and a thickened Congaree relative to other only in the Millhaven core. It is here they are assigned to the cores. Warley Hill Formation (Falls and Prowell, this volume, The Congaree Formation is middle Eocene. It contains chap. A) and to calcareous nannofossil Zone NP 15 (Bybell, two recognizable dinocyst assemblages, which are equiva this volume, chap. F). lent to those found in the upper part of the Tallahatta Forma Middle Eocene sediments correlative with the upper tion and the lower part of the Lisbon Formation in Alabama. part of the Lisbon Formation and the Gosport Sand in Ala The Warley Hill Formation is recognized only in the most bama are present in the Santee Limestone in all cores. basin ward core (Millhaven). Assemblages vary from quite diverse to poorly preserved The Tertiary units in the Burke and Screven County and nondiagnostic. Pentadinium goniferum Edwards is cores studied here show a much more complex history than present in every sample. The lowest occurrences of Cor- was anticipated. In these generally shallow marine sedi dosphaeridium cantharellus (Brosius) Gocht, Cyclopsiella ments, local patterns of erosion and deposition are impor vieta Drugg & Loeblich, and Dapsilidinium pseudocol- tant. A paleo-Savannah River may have wholly or partially ligerum (Stover) Bujak et al. (pi. 1, fig. 18) are found in the eroded units such as the Snapp Formation to allow selective Santee Limestone. Hystrichosphaeropsis Deflandre n. sp, A infilling, or selective preservation of more widespread infill (pi. 3, figs.7-9), Pentadinium Gerlach n. sp. D, and Penta ing, during later transgressions. dinium polypodum Edwards are apparently restricted to the Santee Limestone. Enneadocysta spp., various species of Heteraulacacysta, and a wide variety of areoligeracean TAXONOMIC NOTES forms are present in the more diverse samples. Species of Wetzeliella (pi. 6, fig. 12) are present in a few samples but The species present are listed in Williams and others are not common. (1998) and their taxonomic history is not repeated here. In the Millhaven and Girard cores, the lowest samples Brief synonymies are provided for dinocysts that are pre in the Santee Limestone are barren or nearly so. In the Mill- sented in open or informal nomenclature. Higher level tax haven core, the sample at 346 ft contains the lowest occur onomy is taken from Fensome and others (1993). Taxa are rences of Cordosphaeridium cantharellus (Brosius) Gocht, presented alphabetically by order. For convenience, dates Pentadinium polypodum Edwards, and Samlandia chlamy- are provided with the authors' names for formal taxa; the dophora Eisenack sensu Stover and Hardenbol (1993). works these represent are not included in the references here Here, the lowest occurrence of Cordosphaeridium but may be found in Williams and others (1998). Table 2 cantharellus (Brosius) Gocht approximates the base of cal provides the slide locations of all figured specimens. careous nannofossil Zone NP 17 (Bybell, this volume, chap. Division DINOFLAGELLATA (Butschli 1885) Fensome et al. 1993 F). In the Girard core, the lowest occurrence of Cor Subdivision DINOKARYOTA Fensome et al. 1993 dosphaeridium cantharellus (Brosius) Gocht is just above the base of the Santee Limestone. Class DINOPHYCEAE Pascher 1914 Dinocyst recovery is spotty in sediments of the Barn- Subclass PERIDINIPHYCIDAE Fensome et al. 1993 well unit. In the Millhaven core, samples contain Batiaca- Order GONYAULACALES Taylor 1980 sphaera baculata Drugg, Batiacasphaera compta Drugg, and Cordosphaeridium funiculatum Morgenroth, which ACHILLEODINIUM BIFORMOIDES (EISENACK 1954) EATON 1976 indicate a late Eocene age. In the Girard core, Rhombodin- Plate 1, figures 1-3 ium perforatum (Jan du Chene & Chateauneuf) Lentin & Williams is diagnostic. Both cores contain Charlesdowniea Remarks.—Both relatively smooth forms and those variabilis (Bujak) Lentin & Vozzhennikova (pi. 5, fig. 11). with striate processes are included. In the remaining cores, samples were not taken in Barnwell sediments, except one sample, which was barren (table 1). AMPHOROSPHAERIDIUM1MULTISPINOSUM (DAVEY & WILLIAMS 1966) SARJEANT 1981 Figure 7 shows core-to-core correlations suggested by Plate 1, figure 4 the dinocyst assemblages. Lower Paleocene sediments are present in all cores, but these may be thicker in the updip AREOLIGERA VOLATA DRUGG 1967 cores (McBean, Millers Pond, and Thompson Oak) than in Plate 1, figures the most downdip core (Millhaven). The younger part of the Ellenton is thinnest in the updip cores. AREOSPHAERIDIUM DIKTYOPLOKUM (KLUMPP 1953) EATON 1971 The Snapp Formation is missing from the Thompson Plate 1, figure 6 Oak core and truncated in the McBean core. The Fourmile Branch Formation is recognized only in the Girard and BATIACASPHAERA BACULATA DRUGG 1970 Thompson Oak cores. In the Thompson Oak core, the Plate 1, figure 7 Girard (R4705) SE NW Millhaven McBean (R4664) 8G1GEOLOGYANDPALEONTOLOGYOFFB (R4663) 100 — Depth BARNWELL BARNWELL 200 - AT AS (feet) Sample UNIT 0- ———————— AR AO -J (part)

UNIT (part) BARNWELL 200 - UNIT -1 Al Millers Pond 300 - SANTEE (R4581) _ _ , -AG 100 - Thompson Oak LIMESTONE -H 100- (R4836) -AC SANTEE SAN ILL w -R SANTEE LS. LS. ^V - SANTEE Q 300 - LS. -Y L R - U LS. =Pp G F CONGAREE _^JsiJ**Ja*|sfss~.., , „., _ L !Y' AF 200 - CONGAREE WARLEY -v FM. F ~«!i;g|^i|i»i*«rf CONGAREE wftffsW™¥f5*Ws«*^ - CONGAREE HILL 2oo _ SNAPP --^jip FM isfiflsSfypsisWlllifiiPTwwr'js^ FORMATION — R FORMATION SNAPP 0 CONGAREE - N FM. — D o FOURMILE I" 4UU FOURMILE r ~ H BRANCH FM. ~ r BRANCH FM. -CF, AE 50Q FORMATION COUNTIES,CORESFROM/ESCREVENBURKEANDGEORGI ELLENTON - ELLENTON ..o n — B —————— FM "^"^^^^^ ELLENTON D 1 300 - FM. .,nn - FM. Sp SNAPP SNAPP FM. FORMATION -D _E ^500 - -c° ELLENTON ELLENTON -A GE 0_JO_20 MILES SOUTH ^ FM. ^R^0 600 - 0 10 20 KILOMETERS FORMATION CAROLINA GD - CH GC x / | ^K i Savannah ,-<.-, N.; ^i|——— i— — Rivfir / / *^C."i:4 ( Site \ [ Burke \^C?~~"'^>_ ...^sste,. Approximate location of the paleontological > / f -"^Y \ ( -»«*1 ' break within the Congaree Formation

~~_o ^ >?creven( j/^ Early Paleocene samples~~

~~Figure 7. Correlation diagram by dinocyst assemblages for the five Georgia cores. Datum is the base of the Santee Limestone. DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G19~~

BATIACASPHAERA COMPTA DRUGG 1970 Dinopterygium cladoides Deflandre. Morgenroth, 1966, pi. Plate 1, figures 8, 9 2, fig. 11. Heteraulacacysta sp. Damassa and others, 1990, fig. 5E, F. CARPATELLA CORNUTA GRIGOROVICH 1969 Dinopterygium sp. Stover and Hardenbol, 1993, pi. 12, fig. Plate 1, figure 10 83. CEREBROCYSTA BARTONENSIS BUJAK 1980 DIPHYES COLLIGERUM (DEFLANDRE & COOKSON 1955) Plate 1, figures 12, 13 COOKSON 1965

CORDOSPHAERIDWM CANTHARELLUS DIPHYES FICUSOIDES ISLAM 1983 (BROSIUS 1963) GOCHT 1969 Plate 2, figure 5 Plate 1, figure 14 DISTATODINIUM ELLIPTICUM (COOKSON 1965) EATON 1976 Remarks.—Cordosphaeridium Eisenack 1963 is Plate 2, figure 9 considered here to be the senior taxonomic synonym of Tityrosphaeridium Sarjeant 1981. The holotype of ENNEADOCYSTA STOVER & WILLIAMS 1995 SPP. Cordosphaeridium inodes (Klumpp 1953) Eisenack 1963 Plate 2, figure 6 clearly shows cingular processes in the illustration by Sarjeant (1981, text-fig. 1). Remarks.—Various species of the genus are included.

~~CORDOSPHAERIDIUM FUNICVLATUM MORGENROTH 1966 EOCLADOPYXIS MORGENROTH 1966 N. SP. A Plate 1, figure 11 Plate 2, figure 7~~

CORDOSPHAERIDIUM EISENACK 1963 SPP. Remarks.—The processes resemble those of Poly- sphaeridium zoharyi (Rossignol 1962) Bujak et al. 1980, Remarks.—The species Cordosphaeridium fibrospino- but the separation of the individual paraplates requires sum Davey & Williams 1966, Cordosphaeridium gracile placement in the genus Eocladopyxis Morgenroth 1966. (Eisenack 1954) Davey & Williams 1966, Cordosphaerid ium inodes (Klumpp 1953) Eisenack 1963, and forms FIBRADINIUM ANNETORPENSE MORGENROTH 1968 between these endmembers are not differentiated in this Plate 2, figure 8 study. FIBROCYSTA STOVER & EVITT 1978 SPP. CORRUDINIUMINCOMPOSITUM (DRUGG 1970) STOVER & EVITT 1978 Remarks.—Various species of the genus are included. Plate 1, figure 15 GLAPHYROCYSTA CF. G.7 VICINA (EATON 1976) STOVER & EVITT 1978 CORRUDINIUM SP. I OF EDWARDS (1984) Plate 2, figures 10-15 Plate 1, figure 16 Remarks.—This form is highly variable in the degree Corrudinium sp. I. Edwards, 1984, pi. 2, fig. 1. of development of the marginal flanges. It resembles Mem- Remarks.—Some forms are transitional to Cerebro- branophoridium aspinatum Gerlach 1961 in overall appear cysta bartonensis Bujak 1980. ance, but it is smaller, has less pronounced dorso-ventral compression, and has less prominent flanges. It resembles CRIBROPERIDINIUM GIUSEPPEI and may be transitional with Membranophoridium biloba- (MORGENROTH 1966) HELENES 1984 tum Michoux 1985, which has narrower flanges and no Plate 1, figure 17 development of pericoels other than along the margins. It is CRIBROPERIDINIUM TENUITABULATUM closest to Glaphyrocystal vicina (Eaton 1976) Stover & (GERLACH 1961) HELENES 1984 Evitt 1978. However, the paracingulum may be more pro DAMASSADINIUM CALIFORNICUM nounced, and the details of the dorsal and ventral surfaces (DRUGG 1967) FENSOME ET AL. 1993 may warrant separation. Plate 2, figures 1-3 HAFNIASPHAERA GOODMANII EDWARDS 1982 Remarks.—Both typical and elongate forms are Plate 3, figure 1 included. Remarks.—The illustrated specimen, like most speci DAPSIUDINIUM PSEUDOCOLLIGERUM mens seen, is actually transitional with primitive forms of (STOVER 1977) BUJAK ET AL. 1980 Pentadinium favatum Edwards. Plate 1, figure 18 HAFNIASPHAERA SEPTATA DINOPTERYGIUM CLADOIDES SENSU MORGENROTH 1966 (COOKSON & EISENACK 1967) HANSEN 1977 Plate 2, figure 4 Plate 3, figure 10 G20 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~HETERAULACACYSTA POROSA BUJAK 1980 genus Cribroperidinium Neale & Sarjeant 1962, emend. Plate 3, figures 2, 3 Helenes 1984.~~

~~HETERAULACACYSTA PUSTULOSA JAN DU CHENE MURATODINIUM FIMBRIATUM & ADEDIRAN 1985 (COOKSON & EISENACK 1967) DRUGG 1970 Plate 3, figure 5 NEMATOSPHAEROPSIS DEFLANDRE & COOKSON 1955 SPP.~~

HETERAULACACYSTA DRUGG & LOEBLICH 1967 SPP. Remarks.—Various species of the genus are included. Plate 3, figure 6 OPERCULODINIUM CENTROCARPUM (DEFLANDRE & COOKSON 1955) WALL 1967 Remarks.—The species Heteraulacacysta campanula Plate 3, figure 14 Drugg & Loeblich 1967 and Heteraulacacysta] leptalea Eaton 1976 and poorly preserved specimens of the genus Remarks.—The species name is used in the broad that are unattributable to species are placed here. sense.

HOMOTRYBLIUM ABBREVIATUM EATON 1976 OPERCULODINIUM WALL 1967 SPP. Plate 3, figure 11 Remarks.—Various species of the genus are included. HOMOTRYBLIUM PLECTILUM DRUGG & LOEBLICH 1967 PENTADINIUM FAVATUM EDWARDS 1982 Plate 3, figure 12 Plate 3, figure 15 HOMOTRYBLIUM TENUISPINOSUM DAVEY & WILLIAMS 1966 PENTADINIUM GONIFERUM EDWARDS 1982 HYSTRICHOKOLPOMA CINCTUM KLUMPP 1953 Plate 3, figure 16

~~HYSTRICHOKOLPOMA RIGAUDIAE DEFLANDRE & COOKSON 1955 PENTADINIUM LATICINCTUM GERLACH 1961 SUBSP. LATICINCTUM HYSTRICHOKOLPOMA DEFLANDRE 1935 SPP. Plate 3, figure 17~~

Remarks.—Various species of the genus are included. PENTADINIUM LATICINCTUM GERLACH 1961 (VERM.) Plate 3, figure 18 HYSTRICHOSPHAERIDIUM TUBIFERUM (EHRENBERG 1838) DEFLANDRE 1937 Pentadinium laticinctum subsp. granulatum. Edwards, 1982, HYSTRICHOSPHAEROPSIS DEFLANDRE 1935 N. SP. A pi. 4, figs. 10,11. Plate 3, figures 7-9 Pentadinium laticinctum (vermicular) Gerlach. Edwards, 1984, pi. 2, fig. 4. Remarks.—This small, distinctive form has relatively high septa that are finely serrate distally. Remarks.—Specimens of P. laticinctum Gerlach 1961 with a vermicular surface are separated from P. laticinctum HYSTRICHOSTROGYLON CONINCKII HEILMANN-CLAUSEN 1985 Gerlach 1961 subsp. laticinctum. The vermicular surface differs from the granular surface of Pentadinium laticinctum HYSTRICHOSTROGYLON MEMBRANIPHORUM AGELOPOULOUS 1964 subsp. granulatum Gocht 1969. Plate 3, figure 13 PENTADINIUM MEMBRANACEUM (EISENACK 1965) STOVER & EVITT 1978 LINGULODINIUM MA CHAEROPHORUM (DEFLANDRE & COOKSON 1955) WALL 1967 Plate 4, figure 1

MELITASPHAERIDIUM ASTERIUM PENTADINIUM POLYPODUM ED WARDS 1982 (EATON 1976) BUJAK ET AL. 1980 Plate 4, figure 2 MELITASPHAERIDIUM PSEUDORECURVA TUM (MORGENROTH 1966) BUJAK ET AL. 1980 PENTADINIUM GERLACH 1961 N. SP. D MILLIOUDODINIUM SP. I OF EDWARDS (1984) Plate 3, figures 19-21 Plate 3, figure 4 Remarks.—In this undescribed form of Pentadinium Millioudodinium sp. I. Edwards, 1984, pi. 2, fig. 2. Gerlach 1961, the periphragm in the paracingular region is separated from the endophragm only along the ventral side; Cribroperidinium sp. 2. Damassa and others, 1990, fig. 4C. the wall layers are appressed laterally and dorsally. The wall Cribroperidinium sp. 2. Firth, 1996, pi. 5, figs. 7, 8. surface is smooth. Remarks.—The honeycomb pattern in the intraplate POLYSPHAERIDIUM ZOHARYI (ROSSIGNOL 1962) areas is distinctive. This form now correctly belongs in the BUJAK ET AL. 1980 DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G21

~~ROTTNESTIA BORUSSICA (EISENACK 1954) TRIGONOPYXIDIA GINELLA (COOKSON & EISENACK 1960) COOKSON & EISENACK 1961 DOWNIE & SARJEANT 1965~~

~~SAMLANDIA CHLAMYDOPHORA EISENACK 1954 TUBERCULODINIUM WALL 1967 N. SP. A Plate 4, figure 3 Plate 4, figure 9~~

SAMLANDIA CHLAMYDOPHORA EISENACK SENSU STOVER Remarks.—Only a few specimens of this form were AND HARDENBOL (1993) encountered. It has a broad flange and faintly developed Plate 4, figure 4 tubercules. The multiplate antapical archeopyle clearly indi cates its affinity with Tuberculodinium Wall 1967. Samlandia chlamydophora Eisenack 1954. Stover and Hard- enbol, 1993, pi. 8, fig. 54 a,b. TURBIOSPHAERA CF. T. GALATEA EATON 1976 Plate 4, figure 12 Remarks.—This form has considerably more differen tiation into separate penetabular process complexes than ILanternosphaeridium lanosum Morgenroth 1966. Drugg does the type of S. chlamydophora Eisenack 1954. and Stover, 1975, pi. 5, fig. 2. SPINIFERITES PSEUDOFURCATUS (KLUMPP 1953) Remarks.—The Georgia form resembles Turbio- SARJEANT 1970 sphaera galatea Eaton 1976, but the intratabular processes Plate 4, figure 5 are not as well developed and may form a more or less con SPINIFERITES MANTELL 1850 SPP. tinuous membrane that represents the postcingular and antapical areas. The endocyst may have a distinct apical Remarks.—Various species of the genus are included. boss. It is more elongate than L. lanosum Morgenroth sensu SYSTEMATOPHORA PLACACANTHA Drugg and Stover (1975). (DEFLANDRE & COOKSON 1955) DAVEY ET AL. 1969 MISCELLANEOUS AREOLIGERACEAN FORMS Plate 4, figure 6 Plate 4, figures 13, 14 Remarks.—The species name is used in the broad Remarks.—This category is used for the highly vari sense. The process complexes are highly variable. able plexus that contains members of the genera TECTATODINIUMPELLITUMVfALL 1967 Adnatosphaeridium, Areoligera, and Glaphyrocysta, except Plate 4, figure 8 for the distinctive species listed separately.

Remarks.—The species name is used in the broad Order PERIDINIALES Haeckel 1894 sense. The wall thickness is highly variable. Although some ANDALUSIELLA POLYMORPHA (MALLOY 1972) specimens are assignable to Tectatodinium grande Williams LENTIN & WILLIAMS 1977 et al. 1993, they are clearly only endmembers in a spectrum. Remarks.—Broad forms with two distinct antapical horns were seen. TECTATODINIUMRUGULATUM (HANSEN 1977) MCMINN 1988 Plate 4, figures 10, 11 ANDALUSIELLA SP. AFF. A. POLYMORPHA OF EDWARDS (1980) Plate 5, figures 3, 4 Remarks.—The species name is used in the broad sense. The wall is thicker than the wall in the type specimen. Andalusiella sp. aff. A. polymorpha (Malloy 1972) Lentin & Williams 1977. Edwards, 1980, p. 9, fig. 1. TENUA SP. CF. T. FORMOSA OF KURITA AND MCINTYRE (1995) Andalusiella australinum (Cookson 1965) Lentin & Will Plate 4. figure 7 iams 1977. Kurita and Mclntyre (1995), pi. 1, fig. 12. Tenua sp. cf. T.formosa (Mao & Norris 1988) Lentin & Wil Remarks.—The two antapical horns are fused proxi- liams 1993. Kurita and Mclntyre, 1995, p. 134, pi. 2, mally. At one-third to one-half of the total length of the fig. 15. longer horn, they separate.

Remarks.—Like the specimens reported by Kurita and 1ANDALUSIELLA RHOMBOHEDRA OF Mclntyre (1995), the specimens in the Georgia cores lack EDWARDS AND OTHERS (1984) well-defined paratabulation. This form was encountered in Plate 5, figure 1 three cores in the lowest samples from the Ellenton Forma 1Andalusiella rhombohedra (Benson) Stover & Evitt. Ed tion. In four of the five samples, Carpatella cornuta Grigor- wards and others, 1984, pi. 2, fig. 5. ovich was also present.

THALASSIPHORA PELAGICA (EISENACK 1954) Remarks.—This small, distinctive form could perhaps EISENACK & GOCHT 1960 represent the endocyst only. G22 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

CHARLESDOWNIEA COLEOTHRYPTA (WILLIAMS & DOWNIE Remarks.—The specimens in the Georgia cores, like 1966) LENTIN & VOZZHENNIKOVA 1989 the ones described by Kurita and Mclntyre (1995), lack the CHARLESDOWNIEA VARIABILIS (BUJAK 1980) additional openings on the pericyst that are found in the type LENTIN & VOZZHENNIKOVA 1989 material of Heilmann-Clausen (1985). Plate 5, figure 11 LEJEUNECYSTA ARTZNER & DORHOFER 1978 SPP. Remarks.—The species name is used in the broad Remarks.—Various species of the genus are included. sense. LENTINIA SERRATA BUJAK 1980 DEFLANDREA DELINEATA COOKSON & EISENACK 1965 Plate 5, figure 12 Plate 5, figure 5 PALAEOCYSTODINIUM GOLZOWENSE ALBERTI 1961 Deflandrea cf. D. dartmooria Cookson & Eisenack 1965. Edwards and others, 1984, pi. 1, fig. 7. PALAEOCYSTODINIUM ALBERTI 1961 SPP. Deflandrea cf. D. dartmooria of Edwards and others (1984). Remarks.—Specimens of the genus Palaeocystodinium Edwards, 1989, pi. 1, fig. 6. Alberti in the Georgia cores were not assigned to species if the endocyst was clearly wider than the endocyst in speci Remarks.—This form lacks the broad shoulders char mens assigned to Palaeocystodinium golzowense Alberti. acteristic of Cerodinium dartmoorium (Cookson & Eisen ack 1965) Lentin & Williams 1987. PALAEOPERIDINIUM PYROPHORUM (EHRENBERG 1838) SARJEANT 1967 DEFLANDREA PHOSPHORITICA EISENACK 1938 Plate 5, figure 13 Plate 5, figure 9 PHELODINIUM SP. OF EDWARDS (1989) DEFLANDREA N. SP. AFF.Z). TRUNCATA STOVER Plate 5, figure 10 Plate 5, figure 8 Phelodinium sp. Edwards, 1989, pi. 1, fig. 9. Remarks.—The specimen shown in plate 5, figure 8 is Phelodinium magnificum sensu lato, Edwards, 1996, pi. 1, a rather large, circumcavate form with a granulate endocyst. fig. 12. This form is relatively rare in the Georgia cores studied, but it may be stratigraphically important. Remarks.—Phelodinium sp. of Edwards (1989) has an elongated outline and straight sides on the epicyst; that is, DEFLANDREA CF. D. DIEBELII ALBERTI OF DRUGG (1967) the epicystal shape is neither convex nor concave in the ter Plate 5, figure 6 minology of Bujak and Davies (1983). This morphotype is restricted to the upper Paleocene in Virginia (Edwards, Deflandrea cf. D. diebelii Alberti 1959. Drugg, 1967, p. 16- 1989, 1996) and the Georgia cores. 17, pi. 2, fig. 6. Deflandrea sp. cf. D. diebelii sensu Drugg 1967. Edwards, PHELODINIUM STOVER & EVITT 1978 SPP. 1980, pi. 9, fig. 4. Plate 5, figure 14 Cerodinium speciosum (Alberti 1959) Lentin & Williams 1987. Kurita and Mclntyre, 1995, pi. 1, fig. 1. Remarks.—Specimens from the Georgia cores assigned to Phelodinium Stover & Evitt spp. are of miscel Remarks.—The periphragm is almost smooth (lacking laneous forms, probably several different species, that striations or spinules). broadly are similar to Phelodinium magnificum (Stanley) Stover & Evitt sensu stricto. DRACODINIUM VARIELONGITUDUM (WILLIAMS & DOWNIE 1966) COSTA & DOWNIE 1979 PHTHANOPERIDINIUM COMATUM (MORGENROTH 1966) Plate 5, figure 7 EISENACK & KJELLSTROM 1972 Plate 5, figure 15 ISABELIDINIUM VIBORGENSE SENSU KURITA AND MCINTYRE (1995) PHTHANOPERIDINIUM ECHINATUM EATON 1976 Plate 5, figure 2 Plate 5, figures 16, 17

Peridiniacean cyst sp. C. Edwards, 1980, pi. 9, fig. 11. PSEUDORHOMBODINIUM LISBONENSE WRENN 1996 Peridiniacean cyst sp. C of Edwards (1980). Edwards, 1989, Plate 6, figure 1 pi. 1, fig. 12. Isabelidinium viborgense Heilmann-Clausen 1985. Kurita RHOMBODINIUM DRACO GOCHT 1955 and Mclntyre, 1995, p. 131, pi. 1, figs. 9, 10. Plate 6, figure 2 DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G23

RHOMBODINIUM PERFORATUM (JAN DU CHENE & Cookson & Eisenack 1962. The category includes poorly CHATEAUNEUF 1975) LENTIN & WILLIAMS 1977 preserved specimens and specimens that do not fall into the Plate 6, figure 3 endmember morphotypes of recognized species.

SELENOPEMPHIX NEPHROIDES BENEDEK 1972 ACRITARCHS Plate 5, figure 18 CYCLOPSIELLA VIETA DRUGG & LOEBLICH 1967 SELENOPEMPHIX BENEDEK 1972 SPP. Plate 6, figure 17 Plate 6, figure 4 XENIKOON AUSTRALIS SENSU BENSON (1976) Remarks.—Various species of the genus were seen. Plate 6, figure 18 SENEGALJNIUM MICROGRANULATUM (STANLEY 1965) STOVER & EVITT 1978 Xenikoon australis Cookson & Eisenack. Benson, 1976, p. Plate 6, figure 5 28, pi. 14, fig. 11. Xenikoon australis Cookson & Eisenack. Edwards and oth Remarks.—This species name is used in the broad ers, 1984, pi. l.fig. 6. sense. Incertae sedis 1. Heilmann-Clausen, 1985, p. 26, text-fig. 11; SPINIDINIUM DENSISPINATUM STANLEY 1965 pi. 15, figs. 7-10. Plate 6, figure 8 Xenikoon australis sensu Edwards and others, 1984. Ed wards, 1989, pi. l,fig. 4. Remarks.—This species name is used in the broad sense. Remarks.—As Heilmann-Clausen (1985) pointed out, SPINIDINIUM PULCHRUM (BENSON 1976) this form lacks tabulation and an observable archeopyle. LENTIN & WILLIAMS 1977 Plate 6, figures 6, 10

SPINIDINIUM COOKSON & EISENACK 1962 SPP. REFERENCES CITED Plate 6, figure 9 Benson, D.G., 1976, Dinoflagellate taxonomy and biostratigraphy Remarks.—Specimens from the Georgia cores at the Cretaceous-Tertiary boundary, Round Bay, Maryland: assigned to Spinidinium Cookson & Eisenack spp. are mis Tulane Studies in Geology and Paleontology, v. 12, no. 4, p. 169-233, pis. 1-15. cellaneous forms that do not clearly fall into the endmember morphotypes of recognized species. The illustrated speci Berggren, W.A., Kent, D.V., Swisher, C.C., HI, and Aubry, M.-R, 1995, A revised Cenozoic geochronology and chronostratig- men, recovered from the upper Eocene Barnwell unit, is raphy, in Berggren, W.A., Kent, D.V., Aubry, M.-R, and Hard- probably reworked. enbol, Jan, eds., Geochronology, time scales and global WETZELIELLA ARTICULATA EISENACK 1938 stratigraphic correlation: SEPM (Society for Sedimentary Geology) Special Publication 54, p. 129-212. Plate 6, figures 7, 11 Bujak, J.P., and Davies, E.H., 1983, Modern and fossil Peridini- Remarks.—The species name is used in the broad ineae: American Association of Stratigraphic Palynologists sense. Contribution Series 13, 203 p., 12 pis. Clarke, J.S., Falls, W.R, Edwards, L.E., [Bukry, David,] Frederik- WETZELIELLA EISENACK 1938 SPP. sen, N.O., Bybell, L.M., Gibson, T.G., Gohn, G.S., and Flem Plate 6, figure 12 ing, Parley, 1996, Hydrogeologic data and aquifer interconnection in a multi-aquifer system in coastal plain sed Remarks.—Specimens from the Georgia cores iments near Millhaven, Screven County, Georgia, 1991-95: assigned to Wetieliella Eisenack spp. are miscellaneous Georgia Geologic Survey Information Circular 99, 43 p., 1 pi. forms; many of the specimens are poorly preserved. in pocket. Clarke, J.S., Falls, W.F., Edwards, L.E., Frederiksen, N.O., Bybell, SMALL PERIDINIACEAN FORMS L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, Plate 6, figures 13-16 hydrologic and water-quality data for a multi-aquifer system in coastal plain sediments near Millers Pond, Burke County, Remarks.—The category "small peridiniacean forms" Georgia, 1992-93: Georgia Geologic Survey Information Cir was used for specimens in the Georgia cores that belong to cular 96, 34 p., 1 pi. in pocket. miscellaneous species of the Family Peridiniaceae Ehren- Damassa, S.P., Goodman, O.K., Kidson, E.J., and Williams, G.L., berg 1831. They belong to several genera including Alter- 1990, Correlation of Paleogene dinoflagellate assemblages to bidinium Lentin & Williams 1985, Lentinia Bujak 1980, standard nannofossil zonation in North Atlantic DSDP sites: Senegalinium Jain & Millepied 1973, and Spinidinium Review of Palaeobotany and Palynology, v. 65, p. 331-339. G24 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Drugg, W.S., 1967, Palynology of the upper Moreno Formation N.O., and Krafft, Kathleen, eds., Cretaceous and Tertiary (Late Cretaceous-Paleocene), Escarpado Canyon, California: stratigraphy, paleontology, and structure, southwestern Mary Palaeontographica, ser. B, v. 120, p. 1-71. land, and northeastern Virginia: American Association of ————1970, Some new genera, species, and combinations of phy- Stratigraphic Palynologists Field Trip Volume and Guide toplankton from the lower Tertiary of the Gulf Coast, U.S.A.: book, p. 137-152, pis. 1-4. Proceedings of the North American Paleontological Conven Fensome, R.A., Taylor, F.J.R., Norris, G., Sarjeant, W.A.S., Whar- tion, Chicago, 1969, part G, p. 809-843. ton, D.I., and Williams, G.L., 1993, A classification of living Drugg, W.S., and Loeblich, A.R., Jr., 1967, Some Eocene and Oli- and fossil dinoflagellates: New York, Micropaleontology gocene phytoplankton from the Gulf Coast, U.S.A.: Tulane Press, Special Publication 7, 351 p. Studies in Geology, v. 5, p. 181-194, pis. 1-3. Firth, J.V., 1987, Dinoflagellate biostratigraphy of the Maastricht- Drugg, W.S., and Stover, L.E., 1975, Stratigraphic range charts, ian to Danian interval in the U.S. Geological Survey Albany selected Cenozoic dinoflagellates, in Evitt, W.R., ed., Pro core, Georgia, U.S.A.: Palynology, v. 11, p. 199-216, pis. 1- ceedings of a forum on dinoflagellates held at Anaheim, Cali 3. fornia, October 16, 1973: American Association of ————1996, Upper middle Eocene to Oligocene dinoflagellate Stratigraphic Palynologists Contributions Series 4, p. 73-76, biostratigraphy and assemblage variations in Hole 913B, pis. 1-7. Greenland Sea, in Thiede, Jorn, Myhre, A.M., Firth, J.V, Edwards, L.E., 1977, Range charts as chronostratigraphic hypothe Johnson, G.L., and Ruddiman, W.F., eds., Proceedings of the ses, with applications to Tertiary dinoflagellates: University Ocean Drilling Program, Scientific Results, v. 151, p. 203- of California, Riverside, unpub. dissertation, 188 p. 242. ————1980, Dinoflagellate biostratigraphy: A first look, in Rein- Heilmann-Clausen, Claus, 1985, Dinoflagellate stratigraphy of the hardt, Juergen, and Gibson, T.G., Upper Cretaceous and lower uppermost Danian to Ypresian in the Viborg 1 borehole, cen Tertiary geology of the Chattahoochee River Valley, western tral Jylland, Denmark: Danmarks Geologiske Unders0gelse, Georgia and eastern Alabama, in Frey, R.W., ed., Excursions Serie A, no. 7, p. 1-69, pis. 1-15. in southeastern geology, v. 2: Geological Society of America Kurita, Hiroshi, and Mclntyre, D.J., 1995, Paleocene dinoflagel Annual Meeting (93d), Atlanta, 1980, Field Trip Guidebooks, lates from the Turtle Mountain Formation, southwestern Man p. 424^27, pi. 9. itoba, Canada: Palynology, v. 19, p. 119-136, pis. 1, 2. ————1982, Biostratigraphically important species of Pentadin- Leeth, D.C., Falls, W.F., Edwards, L.E., Frederiksen, N.O., and ium Gerlach, 1961, and a likely ancestor, Hafiiiasphaera Fleming, R.F., 1996, Geologic, hydrologic, and water-chem goodmanii n. sp., from the Eocene of the Atlantic and Gulf istry data for a multi-aquifer system in coastal plain sediments Coastal Plains: Palynology, v. 6, p. 105-117. near Girard, Burke County, Georgia, 1992-95: Georgia Geo ———1984, Dinocysts of the Tertiary Piney Point and Old logic Survey Information Circular 100, 26 p, 1 pi. Church Formations, Pamunkey River area, Virginia, in Ward, Lucas-Clark, Joyce, 1992, Some characteristic fossil dinoflagellate L.W., and Krafft, Kathleen, eds., Stratigraphy and paleontol cysts of Eocene strata, Savannah River Site, South Carolina, ogy of the outcropping Tertiary beds in the Pamunkey River in Fallaw, W.C., and Price, Van, eds., Geological investiga region, central Virginia Coastal Plain—Guidebook for Atlan tions of the central Savannah River area, South Carolina and tic Coastal Plain Geological Association 1984 field trip: Georgia (Carolina Geological Society field trip guidebook, Atlantic Coastal Plain Geological Association, p. 124-134, November 13-15, 1992): U.S. Department of Energy and pis. 1-4. South Carolina Geological Survey, p. CGS-92-B.VII.1- ————1989, Dinoflagellate cysts from the lower Tertiary forma B.VII.6. tions, Haynesville cores, Richmond County, Virginia, chap. C Morgenroth, Peter, 1966, Mikrofossilien uns Konkretionen des of Mixon, R.B., ed., Geology and paleontology of the nordwesteuropaischen Untereozans: Palaeontographica, ser. Haynesville cores—Northeastern Virginia coastal plain: U.S. B,v. 119, p. 1-53, pis. 1-11. Geological Survey Professional Paper 1489, p. C1-C12, pis. Prowell, D.C., Christopher, R.A., Edwards, L.E., Bybell, L.M., and 1-5. Gill, H.E., 1985 [1986], Geologic section of the updip coastal ————1992, Dinocysts from the lower Tertiary units in the Savan plain from central Georgia to western South Carolina: U.S. nah River area, South Carolina and Georgia, in Zullo, V.A., Geological Survey Miscellaneous Field Studies Map MF- Harris, W.B., and Price, Van, eds., Savannah River region; 1737, 10-p. text, 1 sheet. Transition between the Gulf and Atlantic Coastal Plains: Pro Prowell, D.C., Edwards, L.E., and Frederiksen, N.O., 1985 [1986], ceedings of the Second Bald Head Island Conference on The Ellenton Formation in South Carolina—A revised age Coastal Plains Geology, Hilton Head Island, November 6-11, designation from Cretaceous to Paleocene, in Stratigraphic 1990, p. 97-99. notes, 1984: U.S. Geological Survey Bulletin 1605-A, p. -1996, Graphic correlation of the Marlboro Clay and Nan- A63-A69. jemoy Formation (uppermost Paleocene and lower Eocene) of Sarjeant, W.A.S., 1981, A restudy of some dinoflagellate cyst Virginia and Maryland, in Jansonius, J., and McGregor, D.C., holotypes in the University of Kiel collections—II. The eds., Palynology; principles and applications, v. 3: Salt Lake Eocene holotypes of Barbara Klumpp (1953); with a revision City, American Association of Stratigraphic Palynologists of the genus Cordosphaeridiunr. Meyniana, v. 33, p. 97-132. Foundation, p. 989-999. Stover, L.E., and Hardenbol, Jan, 1993 [1994], Dinoflagellates and Edwards, L.E., Goodman, D.K., and Witmer, R.J., 1984, Lower depositional sequences in the lower Oligocene (Rupelian) Tertiary (Pamunkey Group) dinoflagellate biostratigraphy, Boom Clay Formation, Belgium: Bulletin de la Societe beige Potomac River area, Virginia and Maryland, in Frederiksen, de Geologic, v. 102, nos. 1-2, p. 5-77, pis. 1-13. DINOCYST BIOSTRATIGRAPHY OF TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA G25

Williams, G.L., Lentin, J.K., and Fensome, R.A., 1998, The Lentin Wrenn, J.H., 1996, Pseudorhombodinium lisbonense gen. et sp. and Williams index of fossil dinoflagellates—1998 edition: nov., a new dinoflagellate fossil from the Lisbon Formation American Association of Stratigraphic Palynologists Contri- (middle Eocene), Little Stave Creek, Alabama: Palynology, v. bution Series 34, 817 p. 20, p. 209-219.

~~PLATES 1-6 PLATE 1~~

~~[Upper scale bar is for specimens at x 400; lower scale bar is for specimens at x 600. All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. Achilleodinium biformoides (Eisenack) Eaton, Millhaven core (490 ft), Congaree Formation, Screven County, Ga., latero-dorsal view at high focus (X 400). 2. Achilleodinium biformoides (Eisenack) Eaton, Millhaven core (466 ft), Congaree Formation, Screven County, Ga., right-lateral view (X 400). 3. Achilleodinium biformoides (Eisenack) Eaton, Girard core (362-362.3 ft), Congaree Formation, Burke County, Ga., ventral view of dorsal surface (X 400). 4. Amphorosphaeridiuml multispinosum (Davey & Williams) Sarjeant, Girard core (484.1^-84.3 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, optical section (X 400). 5. Areoligera volata Drugg, Millers Pond core (252-257 ft), Ellenton Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). 6. Areosphaeridium diktyoplokum (Klumpp) Eaton, Millhaven core (442 ft), Warley Hill Formation, Screven County, Ga., orientation uncertain, upper focus (X 400). 7. Batiacasphaera baculata Drugg, Millhaven core (205 ft), Barnwell unit, Screven County, Ga., orientation uncertain, upper focus (X 400). 8, 9. Batiacasphaera compta Drugg, Millhaven core (205 ft), Barnwell unit, Screven County, Ga., orientation uncertain; 8, upper focus; 9, slightly lower focus (X 400). 10. Carpatella cornuta Grigorovich, Millhaven core (639.5 ft), Ellenton Formation, Screven County, Ga., ventral view of ventral surface, broken specimen (X 400). 11. Cordosphaeridiumfnniculatum Morgenroth, Millhaven core (205 ft), Barnwell unit, Screven County, Ga.. orientation uncertain, upper focus, fragment (X 400). 12, 13. Cerebrocysta bartonensis Bujak, Millhaven core (490 ft), Congaree Formation, Screven County, Ga., antapical views; 12, antapex; 13, apex (X 400). 14. Cordosphaeridium cantharellus (Brosius), Gocht, Millhaven core (346 ft) Santee Limestone, Screven County, Ga., orientation uncertain, upper focus (X 400). 15. Corrudinium incompositum (Drugg) Stover & Evitt, Girard core (211.1-211.3 ft), Barnwell unit, Burke County, Ga., right-lateral view (X 600). 16. Corrudinium sp. I of Edwards (1984), Millhaven core (466 ft), Congaree Formation, Screven County, Ga., orientation uncertain, upper focus (X 400). 17. Cribroperidinium giuseppei (Morgenroth) Helenes, Millhaven core (346 ft) Santee Limestone, Screven County, Ga., dorsal view of dorsal surface (X 400). 18. Dapsilidinium pseudocolligerum (Stover) Bujak et al., Girard core (211.1-211.3 ft), Barnwell unit, Burke County, Ga., orientation uncertain, upper focus (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G, PLATE 1

~~i I I 0 20 40 jam~~

~~17 0 20 40 jam~~

~~ACHILLEODINIUM, AMPHOROSPHAERIDIUM, AREOLIGERA, AREOSPHAERIDIUM, BATIACASPHAERA, CARPA- TELLA, CORDOSPHAERIDIUM, CEREBROCYSTA, CORRUDINIUM, CRIBROPERIDINIUM. AND DAPSILIDINIUM PLATE 2~~

~~[Upper scale bar is for specimens at x 400; lower scale bar is for specimens at x 600. All specimens are from Screven and Burke Counties, Georgia]~~

Figures 1, 2. Damassadinium californicum (Drugg) Fensome et al., McBean core (294 ft), Ellenton Formation, Burke County, Ga., right-lateral views; 1, upper focus; 2, lower focus (X 400). 3. Damassadinium californicum (Drugg) Fensome et al., Millhaven core (589 ft), Ellenton Formation, Screven County, Ga., right-lateral view, upper focus (X 400). 4. Dinopterygium cladoides sensu Morgenroth (1966), Millhaven core (205 ft), Barnwell unit, Screven County, Ga., interior view of epicyst (x 400). 5. Diphyes ficusoides Islam, Millhaven core (466 ft), Congaree Formation, Screven County, Ga., ventral? view at midfocus (X 400). 6. Enneadocysta Stover & Williams sp., Millhaven core (216.5 ft), Barnwell unit, Screven County, Ga., orientation uncertain, midfocus (X400). 7. Eocladopyxis Morgenroth n. sp. A, Girard core (362-362.3 ft), Congaree Formation, Burke County, Ga., interior view of hypocyst (X 400). 8. Fibradinium annetorpense Morgenroth, Millhaven core (589 ft), Ellenton Formation, Screven County, Ga., right-lateral view, upper focus (X 600). 9. Distatodinium ellipticum (Cookson) Eaton, Millhaven core (210 ft), Barnwell unit, Screven County, Ga., orientation uncertain, midfocus (X 400) 10-12. Glaphyrocysta cf. G.I vicina (Eaton) Stover & Evitt, Millhaven core (466 ft), Congaree Formation, Screven County, Ga., dorsal views; 10, dorsal surface; 11, optical section; 12, ventral surface (x 400). 13. Glaphyrocysta cf. G.I vicina (Eaton) Stover & Evitt, Girard core (362-362.3 ft), Congaree Formation, Burke County, Ga., ventral view of ventral surface (X400). 14. Glaphyrocysta cf. G.I vicina (Eaton) Stover & Evitt, Thompson Oak core (192 ft), Congaree Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). 15. Glaphyrocysta cf. G.I vicina (Eaton) Stover & Evitt, Girard core (321.4-321.6 ft), Santee Limestone, Burke County, Ga., ventral view of ventral surface (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G, PLATE 2

~~0 20 40 |im i___i___i 13 0 20 40 Jim~~

~~DAMASSADINIUM, DINOPTERYGIUM CLADOIDES SENSU MORGENROTH (1966), DIPHYES, ENNEADOCYSTA, EOCLADOPYXIS, FIBRADINIUM, DISTATODINIUM, AND GLAPHYROCYSTA PLATE 3~~

~~[All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. Hafniasphaera goodmanii Edwards, Thompson Oak core (255 ft), Fourmile Branch Formation, Burke County, Ga., dorsal view of dorsal surface (x 400). 2, 3. Heteraulacacysta porosa Bujak, Thompson Oak core (138 ft), Santee Limestone, Burke County, Ga., antapical views; 2, antapex; 3, optical section (X 400). 4. Millioudodinium sp. I of Edwards (1984), McBean core (181 ft), Santee Limestone, Burke County, Ga., left-lateral view, upper focus (x 400). 5. Heteraulacacysta pustulosa Jan du Chene & Adediran, McBean core (181 ft), Santee Limestone, Burke County, Ga., interior view of hypocyst (X 400). 6. Heteraulacacysta Drugg & Loeblich sp., Millhaven core (346 ft), Santee Limestone, Screven County, Ga., apical view, midfocus (X 400). 7-9. Hystrichosphaeropsis Deflandre n. sp. A, Thompson Oak core (138 ft), Santee Limestone, Burke County, Ga., dorsal views; 7, dorsal surface; 8, optical section; 9, ventral surface (X 400). 10. Hafniasphaera septata (Cookson & Eisenack) Hansen, Girard core (517.9-518.1 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, upper focus (x 400). 11. Homotryblium abbreviatum Eaton, Thompson Oak core (269 ft), Fourmile Branch Formation, Burke County, Ga., oblique exterior view of hypocyst (X 400). 12. Homotryblium plectilum Drugg & Loeblich, Girard core (211.1-211.3 ft), Barnwell unit, Burke County, Ga., exterior view of hypocyst (X 400). 13. Hystrichostrogylon membmniphorum Agelopoulous, Thompson Oak core (174 ft), Santee Limestone, Burke County, Ga., orientation uncertain, midfocus (X 400). 14. Operculodinium centrocarpum (Deflandre & Cookson) Wall, Millhaven core (466 ft), Congaree Formation, Screven County, Ga., dorsal view of dorsal surface (x 400). 15. Pentadiniumfavatum Edwards, Millhaven core (473.5 ft), Congaree Formation, Screven County, Ga., dorsal view of dorsal surface (X 400). 16. Pentadinium goniferum Edwards, Millhaven core (346 ft), Santee Limestone, Screven County, Ga., dorsal view of dorsal surface (X 400). 17. Pentadinium laticinctum Gerlach subsp. laticinctum, Millhaven core (210 ft), Barnwell unit, Screven County, Ga., oblique left-lateral view, upper focus (X 400). 18. Pentadinium laticinctum Gerlach (verm.) Millhaven core (210 ft), Barnwell unit, Screven County, Ga., oblique right-lateral view, upper focus (x 400). 19-21. Pentadinium Gerlach n. sp. D, Thompson Oak core (164 ft), Santee Limestone, Burke County, Ga., apical views; 19, apex; 20, optical section; 21, antapex (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G, PLATE 3

~~16 17 18~~

~~I 1~~

~~0 20 40 19 20~~

~~HAFNIASPHAERA, HETERAULACACYSTA, MILLIOUDODINIUM, HYSTRICHOSPHAEROPSIS, HOMOTRYBLIUM, HYSTRICHOSTROGYLON, OPERCULODINIUM, AND PENTADINIUM PLATE 4~~

~~[All specimens are from Screven and Burke Counties, Georgia!~~

Figure 1. Pentadinium membranaceum (Eisenack) Stover & Evitt, Millhaven core (293 ft), Santee Limestone, Screven County, Ga., ventral view of dorsal surface (X 400). 2. Pentadinium polypodum Edwards, Millhaven core (293 ft), Santee Limestone, Screven County, Ga., left-lateral view, upper focus (X 400). 3. Samlandia chlamydophora Eisenack, Thompson Oak core (192 ft), Congaree Formation, Burke County, Ga., dorsal view, midfocus (X 400). 4. Samlandia chlamydophora Eisenack sensu Stover and Hardenbol (1993), Millhaven core (346 ft), Santee Limestone, Screven County, Ga., ventral view of ventral surface (X 400). 5. Spiniferites pseudofurcatus (Klumpp) Sarjeant, Millhaven core (346 ft), Santee Limestone, Screven County, Ga., right-lateral view, upper focus (X 400). 6. Systematophora placacantha (Deflandre & Cookson) Davey et al., Girard core (211.1-211.3 ft), Barnwell unit, Burke County, Ga., apical view, upper focus (X 400). 7. Tenua sp. cf. T. formosa of Kurita and Mclntyre (1995), Girard core (517.9-518.1 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, upper focus (X 400). 8. Tectatodinium pellitum Wall, Girard core (321.4-321.6 ft), Santee Limestone, Burke County, Ga., dorsal view of dorsal surface (X 400). 9. Tuberculodinium Wall n. sp. A, Millhaven core (210 ft), Barnwell unit, Screven County, Ga., antapical view of antapex (X 400). 10, 1 1. Tectatodinium rugulatum (Hansen) McMinn, Girard core (517.9-518.1 ft), Ellenton Formation, Burke County, Ga., ventral views; 10, ventral surface; 1 1, dorsal surface (X 400). 12. Turbiosphaera cf. T. galateaEaton, Millhaven core (490 ft), Congaree Formation, Screven County, Ga., ventral view, midfocus (X 400). 13. Miscellaneous areoligeracean form, Millhaven core (490 ft), Congaree Formation, Screven County, Ga., dorsal view, midfocus (X 400). 14. Miscellaneous areoligeracean form, Millers Pond core (237-242 ft), Ellenton Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G. PLATE 4

~~PENTADINIUM, SAMLANDIA, SPINIFERITES, SYSTEMATOPHORA, TENUA, TECTATODINIUM, TUBERCULODINIUM, TURBIOSPHAERA, AND MISCELLANEOUS AREOLIGERACEAN FORMS PLATE 5~~

~~[Upper scale bar is for specimens at x 300; middle scale bar is for specimens at x 400; lower scale bar is for specimens at x 600. All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. lAndalusiella rhombohedra of Edwards and others (1984), Millers Pond core (237-242 ft), Ellenton Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). 2. Isabelidinium viborgense sensu Kurita and Mclntyre (1995), McBean core (276 ft), Ellenton Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). 3. Andalusiella sp. aff. A polymorpha of Edwards (1980), Millers Pond core (237- 242 ft), Ellenton Formation, Burke County, Ga., mostly dorsal view of dorsal surface (X 300). 4. Andalusiella sp. aff. A. polymorpha of Edwards (1980), Thompson Oak core (281 ft), Ellenton Formation, Burke County, Ga., left-lateral view at midfocus (X 300). 5. Deflandrea delineata Cookson & Eisenack, Millhaven core (589 ft), Ellenton Formation, Screven County, Ga., ventral view of ventral surface (X 400). 6. Deflandrea cf. D. diebelii Alberti of Drugg (1967), Girard core (517.9-518.1 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, midfocus (X 400). 7. Dracodinium varielongitudum (Williams & Downie) Costa & Downie, Girard core (415 ft), Fourmile Branch Formation, Burke County, Ga., ventral view of dorsal surface (X 400). 8. Deflandrea n. sp. aff. D. truncata Stover, Girard core (521-521.2 ft), Ellenton Formation, Burke County, Ga., ventral view at midfocus (X 400). 9. Deflandrea phosphoritica Eisenack, Millhaven core (205 ft), Barnwell unit, Screven County, Ga., dorsal view of dorsal surface (X 400). 10. Phelodinium sp. of Edwards (1989), Thompson Oak core (281 ft), Ellenton Formation, Burke County, Ga., ventral view of dorsal surface (X 400). 11. Charlesdowniea variabilis (Bujak) Lentin & Vozzhennikova, Millhaven core (216.5 ft), Barnwell unit, Screven County, Ga., dorsal view of dorsal surface (X 400). 12. Lentinia serrata Bujak, Girard core (362-362.3 ft), Congaree Formation, Burke County, Ga., ventral view at midfocus (X 400). 13. Palaeoperidiniumpyrophorum (Ehrenberg) Sarjeant, Millhaven core (589 ft), Ellenton Formation, Screven County, Ga., ventral view of dorsal surface (X 400). 14. Phelodinium Stover & Evitt sp., McBean core (276 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, upper focus (X 400). 15. Phthanoperidinium comatum (Morgenroth) Eisenack & Kjellstrom, Millhaven core (216.5 ft), Barnwell unit, Screven County, Ga., ?right-lateral view, upper focus (X 400). 16, 17. Phthanoperidinium echinatum Eaton, Millhaven core (466 ft), Congaree Formation, Screven County, Ga., ventral views; 16, ventral surface; 17, dorsal surface (X 600). 18. Selenopemphix nephroides Benedek, Millhaven core (413 ft), Warley Hill Formation, Screven County, Ga., ?apical view at midfocus (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G, PLATE 5

~~0 20 40 Jim i i i ^" 0 20 40 Jim~~

~~16 17 18 0 20 40 jam~~

~~ANDALUSIELLA, ISABELIDINIUM, DEFLANDREA, DRACODINIUM, PHELODINIUM, CHARLESDOWNIEA, LENTINIA, PALAEOPERIDINIUM, PHTHANOPERIDINWM, AND SELENOPEMPHIX PLATE 6~~

~~[All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. Pseudorhombodinium lisbonense Wrenn, Girard core (362-362.3 ft), Congaree Formation, Burke County, Ga., dorsal view of dorsal surface (X 400). 2. Rhombodinium draco Gocht, Millhaven core (313.5 ft), Santee Limestone, Screven County, Ga., dorsal view at midfocus (X 400). 3. Rhombodinium perforatum (Jan du Chene & Chateauneuf) Lentin & Williams, Girard core (211.1-211.3 ft), Barnwell unit, Burke County, Ga., ventral view at midfocus (X 400). 4. Selenopemphix Benedek sp., Millhaven core (413 ft), Warley Hill Formation, Screven County, Ga., apical view of apex (X 400). 5. Senegalinium microgranulatum (Stanley) Stover & Evitt, Millers Pond core (237- 242 ft), Ellenton Formation, Burke County, Ga., ventral view at midfocus (X 400). 6, 10. Spinidinium pulchrum (Benson) Lentin & Williams, Thompson Oak core (302 ft), Ellenton Formation, Burke County, Ga., ventral views: 6, ventral surface; 10, dorsal surface (X 400). 7. Wetzeliella articulata Eisenack sensu amplo, Millhaven core (490 ft), Congaree Formation, Screven County, Ga., dorsal view, upper focus (X 400). 8. Spinidinium densispinatum Stanley, Girard core (521.0-521.2 ft), Ellenton Formation, Burke County, Ga., dorsal? view of dorsal surface (X 400). 9. Spinidinium Cookson & Eisenack sp., reworked?, Millhaven core (216.5 ft), Barnwell unit, Screven County, Ga., ventral view at midfocus (X 400). 11. Wetzeliella articulata Eisenack sensu amplo, Millhaven core (483.5 ft), Congaree Formation, Screven County, Ga., ventral view at midfocus (X 400). 12. Wetzeliella Eisenack sp., Millers Pond core (124 ft), Santee Limestone, Burke County, Ga., dorsal view of dorsal surface (X 400). 13. Small peridiniacean form, Millhaven core (571 ft), Ellenton Formation, Screven County, Ga., ventral? view of dorsal surface (X 400). 14. Small peridiniacean form, Millhaven core (564-565 ft), Snapp Formation, Screven County, Ga., ventral view of dorsal surface (X 400). 15. Small peridiniacean form, McBean core (276 ft), Ellenton Formation, Burke County, Ga., orientation uncertain, midfocus (X 400). 16. Small peridiniacean form, Millers Pond core (237-242 ft), Ellenton Formation, Burke County, Ga., ventral view at midfocus (X 400). 17. Cyclopsiella vieta Drugg & Loeblich, Millhaven core (205 ft), Barnwell unit, Screven County, Ga., high focus (X 400). 18. Xenikoon australis sensu Benson (1976), Millhaven core (571 ft), Ellenton Formation, Screven County, Ga., midfocus (X 400). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-G, PLATE 6

~~0 20 40 jum~~

~~15 17 18 PSEUDORHOMBODINIUM, RHOMBODINIUM, SELENOPEMPHIX, SENEGALINIUM, SPINIDINIUM, WETZELIELLA, SMALL PERIDINIACEAN FORMS, CYCLOPSIELLA, AND XENIKOON~~

~~U.S. Department of the Interior U.S. Geological Survey~~

~~Pollen Biostratigraphy of Lower Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia By Norman 0. Frederiksen~~

~~U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-H~~

~~Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey~~

~~GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA~~

~~Edited by Lucy E. Edwards~~

~~CONTENTS~~

Abstract ...... HI Introduction ...... 1 Acknowledgments ...... 2 Material and Methods ...... 2 Correlations and Age Determinations ...... 2 Millhaven Test Hole...... 2 Ellenton Formation...... 2 Snapp Formation ...... 6 Congaree Formation ...... 6 Warley Hill Formation ...... 7 Santee Limestone...... 7 BarnwellUnit...... 9 Girard Test Hole ...... 9 Ellenton Formation ...... 9 Snapp Formation ...... 9 Fourmile Branch Formation ...... 9 Congaree Formation...... 9 Santee Limestone ...... 9 BarnwellUnit ...... 9 Thompson Oak Test Hole ...... 12 Ellenton Formation...... 12 Fourmile Branch Formation ...... 13 Congaree Formation...... 13 Santee Limestone ...... 14 BarnwellUnit ...... 14 Millers Pond Test Hole ...... 14 Ellenton Formation...... 14 Snapp Formation ...... 14 Congaree Formation ...... 15 Santee Limestone ...... 15 BarnwellUnit ...... 15 McBean Test Hole ...... 17 Ellenton Formation...... 17 Snapp Formation ...... 17 Congaree Formation ...... 17 Santee Limestone ...... 17 BarnwellUnit ...... 17 Summary ...... 18 References Cited ...... 19

~~PLATES [Plates follow References Cited]~~

~~1,2. Angiosperm pollen grains.~~

~~Ill IV CONTENTS~~

~~FIGURES~~

1. Index map showing the Savannah River Site and the location of test holes for this study ...... H2 2. Pollen zonation chart for the Paleocene of the Eastern United States ...... 6 3-14. Charts showing— 3. Pollen distributions in six samples from the Ellenton Formation in the Millhaven core ...... 7 4. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in samples R4664 GD, B, and D, from 620.8, 581.0, and 571.0 ft, respectively, in the Ellenton Formation in the Millhaven core ...... 8 5. Pollen distributions in four of the five samples from the Ellenton Formation of the Girard core ...... 10 6. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4705 B (from 521.0-521.2 ft) and AD (from 517.9-518.1 ft) from the Ellenton Formation in the Girard core...... 11 7. Pollen distributions in four samples, from 302.0 to 183.0 ft, of the Ellenton and Congaree Formations in the Thompson Oak core ...... 12 8. Known stratigraphic ranges in the eastern Gulf Coast of two biostratigraphically important pollen species found in sample R4836 D, from 281.0 ft, in the Ellenton Formation in the Thompson Oak core...... 13 9. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4836 K, from 192.0 ft, in the Congaree Formation in the Thompson Oak core ...... 14 10. Pollen distributions in three samples between 257.0 and 148.0 ft in the Millers Pond core...... 15 11. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4581 Q, from 252.0-257.0 ft, in the Ellenton Formation in the Millers Pond core ...... 16 12. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4581 U, from 148.0 ft, in the Santee Limestone in the Millers Pond core...... 17 13. Pollen distributions in two samples, from 264.0 and 181.0 ft, in the Snapp Formation and Santee Limestone in theMcBean core...... 18 14. Known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4663 D, from 264.0 ft, in the Snapp Formation in the McBean core ...... 19

~~TABLES~~

1. Samples containing pollen and samples barren of pollen from each stratigraphic unit in each core ...... H3 2. Slide numbers and microscope coordinates of photographed specimens ...... 4 3. List of pollen taxa mentioned in this report followed by the illustration location...... 4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Pollen Biostratigraphy of Lower Tertiary Sediments from Five Cores from Screven and Burke Counties, Georgia

~~By Norman O. Frederiksen~~

ABSTRACT others, 1994, 1996; Clarke and West, 1994; Leeth and oth ers, 1996). The Cretaceous and Cenozoic aquifers are diffi Seventeen biostratigraphically useful lower Tertiary cult to correlate from area to area because of structural samples were examined for their pollen taxa from five test movement and rapid facies changes. Some biostratigraphic holes (Millhaven, Girard, Thompson Oak, Millers Pond, research has been completed toward the goal of correlating and McBean) in Screven and Burke Counties, Georgia. Ten aquifers between some of the test holes (Prowell and others, biostratigraphically useful samples from the Ellenton For 1985; Edwards, 1992; Edwards and Clarke, 1992; Edwards mation have earliest and latest possible ages of late early and Frederiksen, 1992; Lucas-Clark, 1992; Falls and others, Paleocene and late Paleocene, respectively, but most or all 1993, 1997; Clarke and others, 1994, 1996; Leeth and oth of the samples are probably late early or early late Pale ers, 1996; Edwards and others, 1997). However, much bio ocene. One good sample from the Snapp Formation is no stratigraphic study remains to be done in the region. older than earliest late Paleocene and no younger than mid This paper uses Tertiary pollen grains in core samples dle late Paleocene. Four productive samples from the Con- from five Georgia test holes to provide biostratigraphic data garee Formation are not very well dated using pollen, but on both marine and nonmarine sediments in the area. The possible ages are generally from late early to middle middle five Georgia test holes (Millhaven, Girard, Thompson Oak, Eocene. Two samples from the Santee Limestone are poorly Millers Pond, and McBean) in Burke and Screven Counties, dated from pollen within the late early Eocene to middle Ga., are directly across the Savannah River from the SRS. Eocene (or younger?) interval. Details of the Tertiary geologic framework of the region are presented elsewhere (Falls and Prowell, this volume, chap. A). Table 1 summarizes the number of samples containing INTRODUCTION pollen and the number of samples barren of pollen from each stratigraphic unit in each core. The Savannah River Site (SRS) in Aiken, Barnwell, and Allendale Counties, S.C. (fig. 1), has manufactured, dis Pollen grains from terrestrial plants are frequently posed of, and stored a variety of hazardous materials since found in marine and terrestrial rocks. However, the palyno- the early 1950's. The U.S. Geological Survey, in coopera logical preparations of samples from cored strata in the SRS tion with the U.S. Department of Energy and the Georgia region commonly contained much more abundant Geologic Survey of the Georgia Department of Natural dinoflagellates of marine to brackish-water origin Resources, is conducting a study of the subsurface geology, (Edwards, this volume, chap. G) than pollen grains of ter hydrology, and water quality in the vicinity of the SRS. The restrial origin. This dinoflagellate dominance was particu goal of the study is to understand the present and possible larly true of the Eocene rocks and the downdip Paleocene future ground-water flow in the aquifers of the area. Many rocks in the Millhaven and Girard cores. Yet, some Pale test holes have been drilled in Georgia and South Carolina ocene samples from the cores contained abundant pollen to study the flow of ground water in the SRS region (Aad- grains, and some others contained sufficient pollen to make land, 1992; Harris and others, 1992; Strom and others, age determinations of these samples possible by using these 1992; Clarke, 1993; Gellici and Logan, 1993; Clarke and fossils. Hi H2 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 30' 81° 30' Tertiary samples. However, some of the species could not be usefully photomicrographed because of mediocre preserva tion or because the specimens were poorly oriented, crum pled, or partially covered with debris.

~~33° 30' CORRELATIONS AND AGE DETERMINATIONS~~

Correlations and age determinations in this paper are based on many articles on spores and pollen grains from lower Tertiary strata in the Gulf Coast and the Mississippi 33° embayment (Jones, 1962; Elsik, 1968a,b, 1974; Fairchild andElsik, 1969; Nichols and Traverse, 1971; Nichols, 1973; Tschudy, 1973a,b, 1975; Potter, 1976; Frederiksen, 1978, 1980a, 1988, 1991, 1998; Jarzen, 1978; Christopher and others, 1980; Frederiksen and others, 1982), in the Southern Atlantic States (Frederiksen, 1978, 1980b, 1991; Frederik 32° 30' sen and Christopher, 1978; Prowell and others, 1985), and in the Middle Atlantic States (Frederiksen, 1979, 1984, EXPLANATION 1991, 1998). The best pollen-stratigraphic control for the

Test hole site and informal name of site Paleocene and Eocene of eastern North America is in the eastern Gulf Coast. Therefore, in this paper, ages and corre lations are made primarily by using ranges of pollen taxa in Figure 1. Index map showing the Savannah River Site and the the eastern Gulf Coast. Most of the pollen taxa identified in location of test holes for this study. this report (table 3) have been previously illustrated with photomicrographs in the papers listed, and many of the taxa ACKNOWLEDGMENTS are illustrated in plates 1 and 2. Figure 2 shows the pollen zones that have been pro D.W. Engelhardt (University of South Carolina) and posed for the Paleocene of the Eastern United States. No R.A. Christopher (Clemson University) reviewed drafts of such zonation has been proposed for the Eocene of this this paper and provided helpful suggestions for its improve region. ment.

MILLHAVEN TEST HOLE MATERIAL AND METHODS The Millhaven test hole (33X048) was drilled by the The samples discussed in this paper were processed by U.S. Geological Survey at lat 32°53'25" N., long 81°35'43" using normal palynological techniques involving treatment W., near Sylvania, Burtons Ferry 7.5 min quadrangle, with hydrochloric, hydrofluoric, and nitric acids; short cen- Screven County, Ga. (fig. 1). The surface elevation is 110 ft trifugation with soapy water to remove fine material; above sea level. Sixteen Tertiary samples from this core removal of mineral grains by swirling; staining with Bis- were examined for pollen, from the depth interval of 639.5 mark brown; and screening on 8- or 10-micrometer (|jm) to 105.0 ft. Seven contained biostratigraphically useful pol sieves. The residues were mounted in glycerine jelly. len assemblages. Table 2 shows the slide numbers and microscope coor dinates of photographed pollen specimens; the slide desig nations show the sample number with the slide number in ELLENTON FORMATION parentheses. The coordinates locate the specimens on Leitz microscope 871956 at the U.S. Geological Survey, Reston, Nine samples of the Ellenton Formation from 639.5 to Va. On this microscope, the coordinates for the center point 571.0 ft in the Millhaven core were examined for pollen, of a standard 25.4x76.2-millimeter slide are 38.8 and 102.5 and six contained significant assemblages. Samples from for the horizontal and vertical axes. The horizontal coordi 639.5, 632.0-632.2, and 577.0 ft were barren of pollen or nates increase toward the right edge of the stage, and the recovered very poor assemblages. Distributions of pollen vertical coordinates increase toward the front of the stage. taxa in the six productive samples are shown in figure 3. Slides are stored at the U.S. Geological Survey, Reston, Va. All of the pollen taxa in sample R4664 GD, from 620.8 The plates illustrate many of the pollen species found in the ft, have long chronostratigraphic ranges within the Pale- POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H3

Table 1. Samples containing pollen and samples barren of ocene except for the Caryapollenites prodromus group of pollen from each stratigraphic unit in each core. Frederiksen (1991). This group has its range base near the [R numbers are U.S. Geological Survey paleobotanical numbers. Depths top of the Naheola Formation in the eastern Gulf Coast (fig. are in feet below the surface. P column: X = pollen grains are present, 4), in the lower part of the upper Paleocene in calcareous although not necessarily ones that are biostratigraphically important. B nannofossil Zone NP 5 and, by definition, at the base of the column: X = barren of pollen] Caryapollenites prodromus Interval Zone (fig. 2). Nanno R number Depth (ft) Unit P B fossil evidence indicates that this sample lies within the Millhaven core lower part of Zone NP 5 (Bybell, this volume, chap. F). R4664 AV— - - 105 Barnwell X Only three pollen taxa were identified in sample R4664 R4fS64 AT __ 195 Barnwell X GE, from 599.5 ft, and the only useful taxon was the R4664 AR—— 210 Barnwell X Caryapollenites prodromus group. Nannofossil evidence R4f»f>4 AT 260 Santee X indicates that this sample lies within the lower part of Zone T> A ddA 'V 490 Congaree X NP 5 (Bybell, this volume, chap. F). R4664 H— — - 499 Congaree X In sample R4664 A, from 589.0 ft, the only age-diag R4664E— — - 564-565 Snapp X nostic species was Choanopollenites sp. cf. C. consan- R4664 D— — - 571 Ellenton X guineus Tschudy of Frederiksen (1979). This species was R4664 C ___ 577 Ellenton X previously known only from the lowermost part of the R4664AW — 579.5 Ellenton X Aquia Formation of Virginia, which belongs to the lower R4664B— — - 581 Ellenton X part of the Gary a Interval Zone (Frederiksen, 1979, 1991) R4664 A— — - 589 Ellenton X and which has been assigned to calcareous nannofossil R4664 GE—— 599.5 Ellenton X Zone NP 5 (Bybell and Gibson, 1991) of early late Pale R4664 GD — 620.8 Ellenton X ocene age. Sample R4664 A also belongs to nannofossil R4664 CH— - 632 632.2 Ellenton X Zone NP 5 (Bybell, this volume, chap. F); therefore, scanty R4664 GC—— 639.5 Ellenton X evidence suggests that Choanopollenites sp. cf. C. consan- R4664 FO __ 755.0-755.3 Steel Creek X guineus Tschudy of Frederiksen (1979) may in fact be con Girard core R4705 F —— - 322.3 322.5 Santee fined to rocks of NP 5 age. However, because nannofossil X Zone NP 5 includes the upper part of the Caryapollenites R4705 AF 415.2^15.5 FourmileBr. X prodromus Interval Zone as well as the lowermost part of R4705 D— — 484.1^84.3 Ellenton X the Carya Interval Zone, it is possible that Choanopollenites 514-514.3 Ellenton X sp. cf. C. consanguineus Tschudy occurs in both of these R4705 AD — - 517.9-518.1 Ellenton X -- pollen zones. T? A "~lf\^ T5 521 521.2 Ellenton X Sample R4664 B, from 581.0 ft, is no older than the TM7OS A 532.5 532.7 Ellenton X upper part of the lower unnamed member of the Porters Thompson Oak core R4836 O— — - 172 Santee X Creek Formation (latest early Paleocene) in the eastern Gulf R4836 N— — - 174 Santee X Coast, according to the known range base of Plicatopollis R4836M— — 181.5 Santee X - triradiatus (Nichols) Frederiksen & Christopher. The sam R4836 L— — - 183 Congaree X ple from 581.0 ft is no younger than the Nanafalia Forma T?A81fi K" 192 Congaree X tion, which is late but not latest Thanetian (known range top R4836 D—— - 281 Ellenton X of Momipites dilatus Fairchild; fig. 4). The chronostrati- O A Q1£i (~* 302 Ellenton X graphic range of the genus Fried'richipollis Krutzsch is Millers Pond core poorly known because pollen of this genus is very rare. TJ/ICQ1 V 72 77 Barnwell X Nannofossil evidence indicates that this sample lies within TJ/ICQ1 V 82-83 Santee X the lower part of Zone NP 5 (Bybell, this volume, chap. F). R4581 W— — 120 Santee X Sample R4664 AW, from 579.5 ft, contained only rare TJ/ICQ1 \I 124 Santee X angiosperm pollen grains. Among the taxa present (fig. 3), TJ/ICO1 TT 148 Santee X the only one of bio stratigraphic interest was Spinaepollis TJ/|CQ1 C 165 Congaree X spinosus (Potonie) Krutzsch. This species has a range from R4581 Q—— - 252-257 Ellenton X near the NP 4-NP 5 calcareous nannofossil zone boundary McBean core (very low in the upper Paleocene) to the top of the Pale R4663 G— — - 181 Santee X ocene. Nannofossil evidence indicates that this sample lies R4663 F ——— 210 Congaree X within the lower part of Zone NP 5 (Bybell, this volume, T> A z:/ro "c 243 Snapp X chap. F). R4663 D— — - 264 Snapp X Critical range bases and tops of taxa in sample R4664 T> A /T/TO /^ 276 Ellenton X D, from 571.0 ft, are displayed in figure 4. From these data, R4663 B— — - 294 Ellenton X it is apparent that this sample can be assigned to the interval H4 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Figure Slide Coordinates Figure Slide Coordinates Plate 1 Plate 1—Continued 1 ...... R4705 B(l) 58.7x95.0 23 R4836 D(l) 54.9 x 109.2 2—.... R4836K(1) 50.1 x 107.5 24 45.8 x 99.2 3...... R4705D(1) 61.8x111.3 4...... R4663 D(l) 50.0 x 104.7 R4705D(1) 55.9x106.3 5 ...... R4836K(1) 56.3 x 109.0 R4705 A(l) 54.2 x 96.9 6——. R4664D(1) 44.7 x 96.0 R4836D(1) 50.9 x 105.4 7,8 — R4664K(1) 61.4x110.6 R4663 G(l) 49.0 x 100.3 9, 10 - R4664FG(1) 58.7x111.7 R4664A(1) 42.0 x 109.9 11 R4664KU) 59.6x93.3 R4663 D(l) 51.0x104.0 12 ----- R4664FG(1) 57.8x105.7 R4664B(1) 42.2 x 95.0 13 R4705 AE(1) 63.4x95.2 R4581 Q(2) 55.5x99.8 14 R4664 K(l) 56.1x96.8 9- R4836 C(l) 62.4 x 93.6 15 R4663 D(l) 52.5 x 105.2 10 R4705 D(l) 61.0x101.0 16 R4705D(1) 62.0x109.4 11 R4581 U(l) 44.0x110.3 17 R4705D(1) 57.3 x 94.9 12 R4664B(1) 42.2 x 95.0 18 R4836K(1) 58.1 x 104.6 13 R4581 Q(6) 45.7x93.8 19 ..... R4664AW(1) 57.4 x 102.5 14 R4664 D(l) 40.2 x 109.7 20 R4836K(1) 64.1 x 105.8 15 R4664B(1) 44.4 x 102.0 21,22- R4836N(1) 52.4x101.8 16 R4836L(1) 49.7x93.7

~~Table 3. List of pollen taxa mentioned in this report followed by the illustration location. [Most pollen taxa have been previously illustrated by the authors listed]~~

~~Taxon Plate Figure~~

Aesculiidites circumslriatus (Fairchild in Stover and others, 1966) Elsik——————- 23 Bombacacidites nacimientoensis (Anderson) Elsik ——————————————————- 14 Bombacacidites reticulatus Krutzsch ——————————————————————————- 13 Carya <29 jam ———————————————————————————————————————- Carya >28 |um ————————————————————————————————————————— Caryapollenites prodromus group of Frederiksen (1991) ———————————————- Choanopollenites sp. cf. C. consanguineus Tschudy of Frederiksen (1979) ————- 5 Eucommia type (tricolporate) of Frederiksen (1988) —————————————————- 20 Favitricolporites baculoferus (Pflug in Thomson andPflug, 1953) Srivastava 1972- Friedrichipollis sp.—————————————————————————— 12 Holkopollenites chemardensis Fairchild in Stover and others (1966)————————- Holkopollenites sp. A———————————————————————————————————- Ilexpollenites sp. —————————————————————————— 24 Insulapollenites rugulatus Leffingwell —————————————————— 6 Intratriporopollenites pseudinstructus Mai————————————————— Intratriporopollenites sp.—————————————————————————————————- 7 Lanagiopollis cribellatus (Srivastava) Frederiksen—————————————————- 15 Lanagiopollis sp., probably L. hadrodictyus Frederiksen ——————————— 16 POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H5

~~Table 3. List of pollen taxa mentioned in this report followed by the illustration location—Continued.~~

~~Taxon Plate Figure~~

Malvacipollis cf. M. tschudyi Frederiksen of Frederiksen (1988) —————————————————————— 1 18 Milfordia hungarica (Kedves) Krutzsch & Vanhoorne in Krutzsch (1970) ————————————————— 1 2 Milfordia incerta (Pflug & Thomson in Thomson and Pflug, 1953) Krutzsch ——————————————— 1 3 Momipites actinus Nichols & Ott ————————————————————————————— Momipites coryloides Wodehouse ———————————————————————————————————————— 1 5 Momipites dilatus Fairchild in Stover and others (1966) —————————————————————————— 1 6 Momipites strictus Frederiksen & Christopher——————————————————————— Momipites tenuipolus group of Frederiksen and Christopher (1978) ————————————————————— 1 4 Momipites-Plicatopollis-Platycaryapollenites complex of Frederiksen (1979) ——————————————— 1 14 Myrtaceidites sp. —————————————————————————————————————————————————— Nudopollis terminalis (Pflug & Thomson in Thomson and Pflug, 1953) Pflug —————————————— 2 2, 3 Nudopollis thiergartii (Thomson & Pflug) Pflug ——————————————————————— Osculapollisl colporatus Frederiksen —————————————————————————————————————— 2 9 Piolencipollis endocuspoides Frederiksen————————————————————————— Platycarya platycaryoides (Roche) Frederiksen & Christopher———————————————————————— 1 7, 8 Platycarya sp. A of Frederiksen and Christopher (1978)————————————————————- 1 9, 10 Platycarya spp. ——————————————————————————————————————————————————— 1 11-13 Platycaryapollenites sp. aff. P. swasticoidus (Elsik) Frederiksen & Christopher ——————————— Plicatopollis triorbicularis type of Frederiksen and Christopher (1978)—————————————————— 1 15 Plicatopollis triradiatus (Nichols) Frederiksen & Christopher——————————————————— Porocolpopollenites ollivierae (Gruas-Cavagnetto) Frederiksen ————————————————— Pseudolaesopollis ventosus (Potonie) Frederiksen ——————————————————————————————— 2 4 Pseudoplicapollis limitatus Frederiksen ——————————————————————————————————— 2 1 Pseudoplicapollis serenus Tschudy———————————————————————————————————————— 2 8 Retitrescolpites anguloluminosus (Anderson) Frederiksen————————————————— Rousea monilifera Frederiksen ————————————————————————————————— Sparganiaceaepollenites sp. ———————————————————————————————————————————— 1 1 Spinaepollis spinosus (Potonie) Krutzsch ———————————————————————————————————— 1 19 Spinizonocolpites prominatus (Mclntyre) Stover & Evans ——————————————————————————— 1 21, 22 Subtriporopollenites anulatus Pflug & Thomson in Thomson and Pflug (1953)——————————— Symplocosl sp. 1 of Frederiksen (1988) ———————————————————————————— Symplocosl sp. aff. Symplocosl sp. 1 of Frederiksen (1988)———————————————————————— 2 11 "Symplocospollenites spp." of Tschudy (1973a)——————————————————————— Tetracolporopollenites lesquereuxianus (Traverse) Frederiksen————————————————— Tetracolporopollenites megadolium (Potonie) Frederiksen————————————————————— Triatriopollenites sparsus group of Frederiksen (1988) —————————————————————— Tricolpites asper Frederiksen——————————————————————————————————————— Triporopollenites infrequens (Stanley) Frederiksen ——————————————————————— Tru dopollis plenus Tschudy ———————————————————————————————————————————— 2 10 Trudopollis spp. ——————————————————————————————————————————————————— Ulmipollenites krempii (Anderson) Frederiksen ——————————————————————————————— 1 17 Ulmipollenites tricostatus (Anderson) Frederiksen ————————————————————————————— 1 16 H6 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

lug LLJ o N O rr LLJ ^ DC W m CL ? UJ m DC y w o > UJ DC m DC o DC h- uj z> => tr o UJ w w LLJ Q- LL PLATYCARYA PLATYCARYOIDES TUSCAHOMA FM. GRAMPIAN HILLS MEMBER NANAFALIA OSTREA THIRSAE BEDS" CARYA FORMATION GRAVEL CREEK SAND MEMBER COAL BLUFF MARL MBR. CARYAPOLLENITES PRODROMUS NAHEOLA FM. OAK HILL MEMBER MATTHEWS LANDING PORTERS \ MARL MEMBER / TRICOLPITES ASPER CREEK LOWER FORMATION UNNAMED MBR. MCBRYDE LIMESTONE CLAYTON MEMBER PSEUDOPLICAPOLLIS SERENUS

~~PINE FORMATION BARREN MEMBER~~

Figure 2. Pollen zonation chart for the Paleocene of the Eastern United States. Zones were proposed by Frederiksen (1991, 1998). Division of the Tertiary into European stages follows Berggren and others (1995). from the lower part of the upper Paleocene (lower Selan- lower part of calcareous nannofossil Zone NP 5 in this core dian) to the upper part of the upper Paleocene (middle is thought to indicate a real absence of the taxon. Carya <29 Thanetian). The sampled interval from the Ellenton Forma jam is not known to range down to the lower part of Zone NP tion of this core contains the Caryapollenites prodromus 5 in either the eastern Gulf Coast or South Carolina (Fred group of Frederiksen (1991) but no specimens of Gary a <29 eriksen, 1991). jam were found. The latter taxon is common in samples above its range base at about the Midwayan-Sabinian Pro SNAPP FORMATION vincial Stage boundary (fig. 2), which is probably within calcareous nannofossil Zone NP 5. The apparent lack of this One sample, R4664 E, from 564.0-565.0 ft, was exam taxon in the Ellenton samples from the Millhaven core ined from the Snapp Formation in the Millhaven core. This would suggest that this sampled interval belongs to the sample contained rare dinoflagellates (Edwards, this vol Caryapollenites prodromus Interval Zone. However, nanno ume, chap. G) but was barren of pollen grains. fossil evidence indicates that a sample from slightly deeper in this core, from 578.0 ft, is tentatively assignable to Zone CONGAREE FORMATION NP 8 of middle Thanetian age, that is, within the upper half of the upper Paleocene (Bybell, this volume, chap. F), Two samples were examined from the Congaree which is well within the range of Carya <29 jam. Thus, the Formation in the Millhaven core. Sample R4664 H, from apparent lack of this taxon in the sample from 571.0 ft is of 499.0 ft, was barren of palynomorphs. Sample R4664 K, a no biostratigraphic significance. On the other hand, the lack fossiliferous sand from 490.0 ft, contained calcareous of Carya <29 jam in the Ellenton samples assigned to the nannofossils of lower to middle Eocene Zone NP 14 POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H7

~~§ Q) .C 3 c5 TO y a. g E o 8 •$ UJ 2 ° 2 ^; J.i.i! I > s § lltHIM^tiJi!" 1 ! a Till- 3 t §|8tlaiMlita8|i|i CO Q ^ LL mOSQ.I^Ol-CQSa.SLL-jSCO^SQ:~~

~~D -i-571.0 < t 4 t 4 1 < ) 4" 4 1 0 4 t Q • • -"Z— » F~~

~~AW - 579 5 \ ^j~-\ < 1 • B - "581.0 4 t < » „ . : : < »~~

~~A -589.0 \ <~\ ELLENTON GE - -599.5 4 1 4 1 ( •~~

~~^£=L~~

~~fiD - ^fipn R~~

~~EXPLANATION~~

~~BClay~~

~~K!| Sandy clay~~

~~[=d| Sandy limestone~~

~~I ~~| Shells present~~

Figure 3. Chart showing pollen distributions in six samples from the Ellenton Formation in the Millhaven core. P indicates that the identification of the species was probable; Q indicates that the identification of the species was uncertain.

(Bybell, this volume, chap. F) and middle Eocene WARLEY HILL FORMATION dinoflagellates (Edwards, this volume, chap. G) but only No samples from the Warley Hill Formation in the sparse pollen grains. Among the pollen taxa recovered were Millhaven core were examined for pollen. Platycarya platycaryoides (Roche) Frederiksen & Christopher and the Momipites-Plicatopollis-Platycary- SANTEE LIMESTONE apollenites complex of Frederiksen (1979). Both taxa have long chronostratigraphic ranges in the lower and middle One sample from the Santee Limestone in the Mill- Eocene, and both have their range bases a short stratigraphic haven core, R4664 AL, from 260.0 ft, was examined for distance below the top of the Paleocene. pollen. However, the sample was barren of these fossils. H8 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~QQ" O~~

~~Q. 2 QCD" O) I LU LU O I O I| •$ ^c ^ "5 Ic .J2 to CD ^ **5 Q t-i VJ £T LLJ h- •I- t -I- §- m Q_ Z < LLI cc So > ^ 5 6cc CD DC O DC ^g LLJ us D Z) DC O C/D LLI Q. LL~~

~~GRAMPIAN HILLS MEMBER NANAFALIA~~

FORMATION GRAVEL CREEK SAND MEMBER COAL BLUFF MARL MBR NAHEOLA FM. OAK HILL MEMBER MATTHEWS LANDING PORTERS s _ _ JVLARL._..MEMBER _ / CREEK LOWER FORMATION UNNAMED MBR, MCBRYDE LIMESTONE CLAYTON MEMBER

~~P ' NE FORMATION BARREN MEMBER~~

Figure 4. Chart showing known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in samples R4664 GD, B, and D, from 620.8, 581.0, and 571.0 ft, respectively, in the Ellenton Formation in the Millhaven core. Samples in which each taxon was found are indicated by the sample initial following the taxon name; an asterisk following the name Momipites actinus indicates that this species was only tentatively identified. POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H9

BARNWELL UNIT contamination of the sample. Dinoflagellates in the samples from 521.0-521.2 ft and 517.9-518.1 ft indicate an early Sample R4664 AR, a fossiliferous sand from 210.0 ft Paleocene, Danian age (Edwards, this volume, chap. G). in the Millhaven core, is from the Barn well unit; the sample Leeth and others (1996) interpreted the data as indicating contained calcareous nannofossils of upper Eocene Zone that these samples are late Paleocene and contain reworked NP 19/20 (Bybell, this volume, chap. F) and typical Eocene early Paleocene palynomorphs. However, it now seems to Oligocene pollen species such as Momipites coryloides more likely that Myrtaceidites sp., Caryapollenites Wodehouse, Pseudolaesopollis ventosus (Potonie) Frederik- prodromus group, and Sparganiaceaepollenites sp. are all sen, and Tetracolporopollenites lesquereuxianus (Traverse) contaminants from uphole, and that the samples from Frederiksen. However, all of these pollen taxa have such 521.0-521.2 ft and 517.9-518.1 ft are early Paleocene in long chronostratigraphic ranges that they are not useful for age and assignable to the Pseudoplicapollis serenus Interval age determinations. Two additional samples of the Barn well Zone (fig. 2). unit, from 195.0 and 105.0 ft, were barren of pollen. Sample R4705 D, from 484.1^84.3 ft, contained a variety of pollen taxa (fig. 5), but all of them are long rang GIRARD TEST HOLE ing within the Paleocene. Dinoflagellates in the sample were interpreted by Leeth and others (1996) and Edwards The Girard test hole was drilled by the U.S. Geological (this volume, chap. G) as indicating an early late Paleocene Survey in southern Burke County at the lookout tower on (Selandian) age. Griffins Landing Road, 2 miles north of the town of Girard, at lat 33°03'54" N., long 81°43'13" W., Girard 7.5 min quad rangle (fig. 1). The surface elevation is 250 ft above sea SNAPP FORMATION level. Seven Tertiary samples from this core were examined for pollen, from the depth interval of 532.7 to 322.3 ft. No pollen samples were examined from the Snapp For mation in the Girard core. ELLENTON FORMATION FOURMILE BRANCH FORMATION Five samples from the Ellenton Formation of the Girard core were examined for pollen. One of these, sample Sample R4705 AE, from 415.2-415.5 ft in the Girard R4705 A, from 532.5-532.7 ft, contained only two taxa (fig. core, is from the Fourmile Branch Formation; the sample 5), both long ranging. The second sample, R4705 C, from contained very rare pollen grains. However, two of the spec 514.0-514.3 ft (not shown in fig. 5), had only very rare pol imens identified were of Platycaryapollenites sp. aff. P. len grains. swasticoidus (Elsik) Frederiksen & Christopher and, there Samples R4705 B, from 521.0-521.2 ft, and AD, from fore, are Eocene. These two specimens are probably of early 517.9-518.1 ft, included taxa listed in figure 5. Stratigraphic Eocene or possibly early middle Eocene age. ranges of the key pollen taxa in the two samples are shown in figure 6. The overlap of ranges of Osculapollisl colporatus Frederiksen and Caryapollenites prodromus group of CONGAREE FORMATION Frederiksen (1991) might suggest that the samples correlate with the Naheola Formation of the eastern Gulf Coast and No pollen samples were examined from the Congaree are early late Paleocene in age. However, two specimens Formation in the Girard core. were found in the sample from 521.0-521.2 ft that might belong to the early Paleocene species Pseudoplicapollis serenus Tschudy. If P. serenus Tschudy actually is present, that might complicate the age interpretation because this species SANTEE LIMESTONE is not known to coexist with the late Paleocene taxon Caryapollenites prodromus group of Frederiksen (1991). One sample of the Santee Limestone, R4705 F, from However, P. serenus Tschudy ranges down into the Creta 322.3-322.5 ft in the Girard core, was examined, but the ceous (fig. 6) and, therefore, might be reworked. sample contained only rare pollen grains. Sparganiaceaepollenites sp. is an upper Paleocene to Holocene(?) species that is probably a result of drilling mud contamination of the sample. Myrtaceidites is a mainly BARNWELL UNIT Eocene to Oligocene genus in southeastern North America and is extremely rare below the Eocene. Therefore, this No pollen samples were examined from the Barnwell specimen also is probably a result of drilling mud unit in the Girard core. H10 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

SAMPLESOFSERIESR47053 Caryapollenitesprodromusgroup Holkopolleniteschemardensis Sparganiaceaepollenitessp. Bombacaciditesreticulatus Pseudoplicapollisserenus(?) Subtriporopollenitesanulatus Favitricolporitesbaculoferus LU Osculapollis?colporatus c g UJ Nudopollisterminalis S I -s U.

~~z FORMATION LITHOLOGY I CL 'a LU Q 484.1- 484.3 — —~~

~~.— . I l~I I -I ELLENTON I I , l-r i i 517.9- I I ABD = 518.1 "521.0- o II • • S S S S !I. 521.2 x 532.5- A - 539 7 ^LT O <'~~

~~EXPLANATION~~

~~BClay~~

~~HH| Sandy clay ^G| Sandy limestone~~

~~, Sand | "~| Shells present~~

Figure 5. Chart showing pollen distributions in four of the five samples from the Ellenton Formation of the Girard core. A fifth sample, not shown, contained only very rare pollen grains. POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA Hll

I O) ^ u. § CO c CO 1 p a CD CO >parganiaceaepollenii "o.CO )sct//apo///s?colporc laryapollenitesprodi fyrtaceiditessp. 1 C75 LU O < OF; n DC W DC I LLI =5 CD CD y£g CO DC CD DC O DC O CO LU =) =) DC O LLI C/) C/5 LLI Q_ LL

~~TUSCAHOMA FM.~~

SELAND.?THANETIAN GRAMPIAN HILLS MEMBER jSABINIAN NANAFALIA UPPER "OSTREA THIRSAE BEDS" FORMATION GRAVEL CREEK SAND MEMBER PALEOCENE COAL BLUFF MARL MBR. NAHEOLA FM. OAK HILL MEMBER . MATTHEWS LANDING PORTERS \ MARL MEMBER / CREEK LOWER MIDWAYAN! FORMATION UNNAMED MBR. MCBRYDE LOWER DANIAN LIMESTONE CLAYTON MEMBER

~~PINE FORMATION BARREN MEMBER~~

Figure 6. Chart showing known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4705 B (from 521.0-521.2 ft) and AD (from 517.9-518.1 ft) from the Ellenton Formation in the Girard core. H12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~O) co LJLJ 5 cc LJLJ 0)~~

~~CD 2 .2 CO .jx 00 DC ffl~~

CD 0 SAMPLESCr-s |DEPTH,IN 0 H _i < oii-siisf.!! $I '$ 1 -i- co $ ^ §- 0 ^ •^ & %%'.§.'•§'§•&£ §- :«3- g o § ^ :§-S "5, T. DC b 0 = 8 9- -i 42 ££« g _J LJ- 1 1 1 1 1 II I ! 1 1i S 1 1 US! ri p i»^;.u

~~CONGAREE ?~~

~~~^ FOURMILE BRANCH — D - 281 .0 ~- ELLENTON -f'^- C, - -302.0~~

~~EXPLANATION Clay Sandy clay I— I Clayey sand Sand~~

Figure 7. Chart showing pollen distributions in four samples, from 302.0 to 183.0 ft, of the Ellenton and Congaree Formations in the Thompson Oak core. P indicates that the identification of the species was probable.

~~THOMPSON OAK TEST HOLE ELLENTON FORMATION~~

The Thompson Oak test hole was drilled by the Geor Two pollen samples were examined from the Ellenton gia Geologic Survey at lat 33°10'42" N., long 81°47'10" W., Formation in the Thompson Oak core. Sample R4836 C, Shell Bluff Landing 7.5-min quadrangle, Burke County, Ga. from 302.0 ft, contained mainly long-ranging taxa. How (fig. 1). The surface elevation is 240 ft. Seven Tertiary sam ever, several specimens were observed of Osculapollisl ples from this core were examined for pollen, from a depth colporatus Frederiksen, whose range in the eastern Gulf interval of 302.0 to 172.0 ft. Pollen distributions in four pro Coast is from the upper part of the lower Paleocene to very ductive samples from this core are shown in figure 7. low in the upper Paleocene (fig. 6). POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H13

~~CO 8 o p.~~

~~.CO "6 CO W Z HI < O .0. E LLJ o LJJ Or < LU cB 0005 D:O or o D =) O 05 HI LL~~

~~GRAMPIAN HILLS MEMBER NANAFALIA~~

~~FORMATION GRAVEL CREEK SAND MEMBER COAL BLUFF MARL MBRp NAHEOLA FM. OAK HILL MEMBER MATTHEWS LANDING PORTERS \ MARL MEMBER LOWER Q_ CREEK FORMATION UNNAMED MBR MCBRYDE LIMESTONE CLAYTON MEMBER~~

~~PINE FORMATION BARREN MEMBER~~

Figure 8. Chart showing known stratigraphic ranges in the eastern Gulf Coast of two biostratigraphically important pollen species found in sample R4836 D, from 281.0 ft, in the Ellenton Formation in the Thompson Oak core.

Most of the taxa in sample R4836 D, from 281.0 ft, CONGAREE FORMATION have long stratigraphic ranges within the Paleocene. The presence of Aesculiidites circumstriatus (Fairchild) Elsik Two pollen samples were examined from the Congaree and Piolencipollis endocuspoides Frederiksen indicates that Formation in the Thompson Oak core. Sample R4836 K, the sample could be any age within the late Paleocene (fig. from 192.0 ft, contained several pollen taxa having some 8). what restricted ranges (figs. 7, 9). The known range ofMal- vacipollis cf. M. tschudyi Frederiksen of Frederiksen FOURMILE BRANCH FORMATION (1988), the most age-definitive species in the sample, is from the lower part of the Tallahatta Formation (Zone NP No pollen samples were examined from the Fourmile 12, middle lower Eocene) to the lower part of the Lisbon Branch Formation in the Thompson Oak core. Formation (Zone NP 15 or lowermost Zone NP 16, lower H14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~-S- 5, SANTEE LIMESTONE~~

Samples R4836 M (181.5 ft), R4836 N (174.0 ft), and Lu Og co £, 2 R4836 O (172.0 ft) were examined for pollen from the San- tee Limestone in the Thompson Oak core, but they con hr co 03 CD s- i z c >> tained no biostratigraphically useful taxa. Spinizonocolpites CO -7 -f o 3 ** v M 1 ^-

~~'mplocos?sp squereuxianui CL CL o V) o O) CL 0) O) 1 o 5 "3 •2 Q. 1 05 ^1 O) .s c Q. § 1 3 ft -2~~

Bombacaciditesreticui "Symplocospollenitess Triporopollenitesinfrec Momipitescoryloides Momipitestenuipolus Porocolpopollenitesoil Pseudoplicapollissere Triatriopollenitesspars Caryapollenitesprodrc Nudopollisterminalis Subthporopollenitesai Symplocos?aff.sp. Tetracolporopollenites Holkopolleniteschema HolkopollenitesAsp. E Rouseamonilifera Thcolpitesasper a CO CM A

~~,-148 iii f SANTEE LMST.^1 :-:vv:-;.v-: CONGAREE 165 — — ^ Q • •~~

~~^>-<^~~

~~~2^-- SNAPP~~

~~252- — __ ELLENTON Q 257~~

~~EXPLANATION~~

~~Limestone~~

~~Figure 10. Chart showing pollen distributions in three samples between 257.0 and 148.0 ft in the Millers Pond core. Q indicates that the identification of the species was uncertain.~~

CONGAREE FORMATION (lower middle Eocene, lower Lutetian) in Alabama and Georgia. However, the true range of this species is poorly Sample R4581 S, from 165.0 ft, is just above the con known. Dinoflagellates in the sample indicate correlation tact of the Snapp and Congaree Formations in the Millers with the upper part of the Lisbon Formation (middle part of Pond core. The sample contained only a few pollen taxa the middle Eocene; Edwards, this volume, chap. G). Three (fig. 10). Either these taxa are long ranging, or else the iden additional samples of the Santee Limestone, from 124.0, tification of the taxa was uncertain. 120.0, and 82.0-83.0 ft, were also examined, but they were either barren of pollen or else did not contain any biostrati- SANTEE LIMESTONE graphically useful taxa.

Sample R4581 U, from 148.0 ft in the Santee Lime stone of the Millers Pond core, had two pollen taxa that do BARNWELL UNIT not range below the lower Eocene part of the Tallahatta For mation in the eastern Gulf Coast (fig. 12). Symplocosl sp. 1 One sample from the Barnwell unit in the Millers Pond of Frederiksen (1988) is a rare species that has previously core was examined for pollen—sample R4581Y from 72.0- been found only in the lower part of the Lisbon Formation 77.0 ft, but it was barren of palynomorphs. H16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~I O)~~

~~§ fo co~~

~~.CO "o II .1 CD HI < ^ rr LLJ ^ 5- 1 CO fi 0. 2 w co O > CC CO CC O CL LLI => => CC O lil CO CO LLI Q. u_~~

~~TUSCAHOMA FM. GRAMPIAN HILLS MEMBER NANAFALIA "OSTREA THIRSAE BEDS"~~

~~FORMATION GRAVEL CREEK SAND MEMBER COAL BLUFF MARL MBR NAHEOLA FM. OAK HILL MEMBER MATTHEWS LANDING . PORTERS \ MARL MEMBER / CREEK LOWER FORMATION UNNAMED MBR MCBRYDE LIMESTONE CLAYTON MEMBER~~

~~PINE FORMATION BARREN MEMBER~~

Figure 11. Chart showing known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4581 Q, from 252.0-257.0 ft, in the Ellenton Formation in the Millers Pond core. POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H17

MCBEAN TEST HOLE The McBean test hole (GGS-3757) was drilled by the Georgia Geologic Survey at lat 33°13'38" N., long 81°55'50" W., in the McBean 7.5-min quadrangle, Burke County, Ga. (fig. 1). The surface elevation is 297 ft above fnCr sea level. Six Tertiary samples from this core were exam ined for pollen, from the depth interval of 294.0 to 181.0 ft. LJJ LJJ CO Two samples contained more than rare pollen grains. These 0 "£•S-! o 2 two samples were from 264.0 and 181.0 ft (fig. 13). -2 £ g "o E Q. (n Z i'£ CO ROPEAN o tracolporop o BSERIES OVINCIAL E CO ELLENTON FORMATION CM 1 (n cc A uu CD 8 1 CO Two samples were examined from the Ellenton Forma cc DC 3 tion (R4663 B and C, from 294.0 and 276.0 ft, respectively) LJJ D D cc O I (n (n LJJ DL LJL iS fi 5 CO in the McBean core, but they were barren or nearly barren of pollen grains.

LISBON SNAPP FORMATION z FORMATION MIDDLE < LLJ (PART) No dinocysts were found in sample R4663 D, from 264.0 ft in the Snapp Formation of the McBean core. The _l fflCLAIBORNIAN critical pollen taxa in this sample (fig. 14) were Momipites dilatus Fairchild and Caryapollenites prodromus group of Frederiksen (1991), whose overlapping ranges indicate that EOCENE TALLAHATTA the sample is no older than earliest late Paleocene and no younger than middle late Paleocene. The sample belongs somewhere within the Caryapollenites prodromus or Carya FORMATION Interval Zones (fig. 2). Sample R4663 E, from 243.0 ft, was YPRESIAN barren or nearly barren of pollen grains. LOWER

~~CONGAREE FORMATION~~

~~Z < HATCHETIGBEE/ Sample R4663 F, from 210.0 ft in the Congaree Forma z BASH I tion of the McBean core, was barren or nearly barren of pol m < FORMATION len grains. CO~~

Figure 12. Chart showing known stratigraphic ranges SANTEE LIMESTONE in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4581 U, from Sample R4663 G, from 181.0 ft in the Santee Lime 148.0 ft, in the Santee Limestone in the Millers Pond stone of the McBean core, contained few pollen taxa (fig. core. 13); however, Ilexpollenites Potonie and Tetracolporopolle- nites rnegadolium (Potonie) Frederiksen are known only from Eocene and younger strata.

~~BARNWELL UNIT~~

~~No pollen samples were examined from the Barnwell unit in the McBean core. H18 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA~~

Q.3 CO o megadolium LU , o ra CO ^5 c CD CD DC LU Insulapollenitesrugul, Momipitestenuipolus Nudopollisterminalis Plicatopollistriorbicul. Pseudolaesopollisve LU Aesculiiditescircumsl Caryapollenitesprodr Porocolpopollenitesc Tetracolporopollenites LL LL Momipitesdilatus Momipitesstrictus Trudopollisplenus 0 . -z. llexpollenitessp. Z CO O o LU CD I DL 1- O DL 1-I DC ^ LU O CO Q _i LL

~~G-i-181~~

~~CONGAREE~~

~~SNAPP D -1- 264 ^"-^_ _~~

~~EXPLANATION~~

~~FT^/1 Sand N^ Sandy limestone~~

Figure 13. Chart showing pollen distributions in two samples, from 264.0 and 181.0 ft, in the Snapp Formation and Santee Limestone in the McBean core. Q indicates that the identification of the species was uncertain.

SUMMARY Only one productive sample was obtained from the Snapp Formation; it was from the McBean core. This sam ple is no older than earliest late Paleocene and no younger Seventeen biostratigraphically useful lower Tertiary than middle late Paleocene. samples were examined for pollen from five cores One productive sample was obtained from the Four- (Millhaven, Girard, Thompson Oak, Millers Pond, and mile Branch Formation, from the Girard core. The sample McBean) in Screven and Burke Counties, Ga. Ten appears to be early Eocene or possibly early middle Eocene biostratigraphically useful samples from the Ellenton in age. Formation were analyzed, from the Millhaven, Girard, Three productive samples were obtained from the Con- Thompson Oak, and Millers Pond cores. Most samples are garee Formation from the Millhaven and Thompson Oak not older than early late Paleocene, but one or two of them cores. The pollen taxa in these samples mainly have long are older—late early Paleocene in age. The youngest stratigraphic ranges within the lower and middle Eocene. possible age for some of the Ellenton samples is more However, one of the samples from the Thompson Oak core difficult to establish. On the basis of pollen evidence, appears to be late early to early middle Eocene in age. several of the Ellenton samples might be as young as middle Two productive samples were examined from the San- late or even late late Paleocene. However, most of the tee Limestone from the Millers Pond and McBean cores. samples are probably not younger than the Caryapollenites These are poorly dated within the late early Eocene to mid prodromus Interval Zone of early late Paleocene age. dle Eocene (or younger?) interval. POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H19

~~I O) e I Lug 3£ to .CD~~

~~CO I"o tt Z < £ o CL .§. VJ LU D- £: LLI e I CD o I CC CD CC O CL ^ £ LU D ID CC O LU CO CO LU CL~~

~~TUSCAHOMA FM.~~

SELAND.?THANETIAN !SABINIAN, GRAMPIAN HILLS MEMBER NANAFALIA UPPER 'OSTREA THIRiJ/4E BEDS" FORMATION 4UIIIIII GRAVEL CREEK SAND M[EMBER PALEOCENE COAL BLUFF MARL MBR. NAHEOLA FM. OAK HILL MEMBER MATTHEWS LANDING PORTERS \ MARL MEMBER / CREEK LOWER 1MIDWAYAN FORMATION UNNAMED MBR. MCBRYDE LOWER DANIAN LIMESTONE CLAYTON MEMBER

~~PINE FORMATION BARREN MEMBER~~

Figure 14. Chart showing known stratigraphic ranges in the eastern Gulf Coast of biostratigraphically important pollen species in sample R4663 D, from 264.0 ft, in the Snapp Formation in the McBean core.

REFERENCES CITED Bybell, L.M., and Gibson, T.G., 1991, Calcareous nannofossils and foraminifers from Paleocene and Eocene strata in Maryland Aadland, R.K., 1992, Hydrogeologic characterization of the, Creta and Virginia, in Gibson, T.G., and Bybell, L.M., leaders, Pale- ceous-Tertiary coastal plain sequence at Savannah River Site, ocene-Eocene boundary sedimentation in the Potomac River South Carolina, in Zullo, V.A., Harris, W.B., and Price, Van, Valley, Virginia and Maryland: I.G.C.P. (International Geo eds., Savannah River region; Transition between the Gulf and logical Correlation Programme) Project 308 Field Trip Guide Atlantic Coastal Plains: Proceedings of\he Second Bald Head book, p. 15-29. Island Conference on Coastal Plains Geology, Hilton Head Christopher, R.A., Prowell, D.C., Reinhardt, J., and Markewich, Island, November 6-11, 1990, p. 62-67. H.W., 1980, The stratigraphic and structural significance of Berggren, W.A., Kent, D.V., Swisher, C.C., III, and Aubry, M.-P, Paleocene pollen from Warm Springs, Georgia: Palynology, v. 1995, A revised Cenozoic geochronology and chronostratig- 4, p. 105-124. raphy, in Berggren, W.A., Kent, D.V, Aubry, M.-P, and Hard- Clarke, J.S., 1993, Conceptual models of possible stream-aquifer enbol, Jan, eds., Geochronology, time scales and global relations in the vicinity of the Savannah River Site, Georgia stratigraphic correlation: SEPM (Society for Sedimentary and South Carolina [abs.]: Geological Society of America Geology) Special Publication 54, p. 129-212. Abstracts with Programs, v. 25, no. 4, p. 8. H20 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Clarke, J.S., Falls, W.F., Edwards, L.E., [Bukry, David,] Frederik- [abs.]: Geological Society of America Abstracts with Pro sen, N.O., Bybell, L.M., Gibson, T.G., Gohn, G.S., and Flem grams, v. 25, no. 4, p. 14. ing, Parley, 1996, Hydrogeologic data and aquifer Frederiksen, N.O., 1978, New Paleogene pollen species from the interconnection in a multi-aquifer system in coastal plain sed Gulf and Atlantic Coastal Plains: U.S. Geological Survey iments near Millhaven, Screven County, Georgia, 1991-95: Journal of Research, v. 6, p. 691-696. Georgia Geologic Survey Information Circular 99, 43 p., 1 pi. ———1979, Paleogene sporomorph biostratigraphy, northeastern in pocket. Virginia: Palynology, v. 3, p. 129-167. Clarke, J.S., Falls, W.F., Edwards, L.E., Frederiksen, N.O., Bybell, ———1980a, Lower Tertiary sporomorph biostratigraphy: Prelimi L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, nary report, in Reinhardt, Juergen, and Gibson, T.G., Upper hydrologic and water-quality data for a multi-aquifer system Cretaceous and lower Tertiary geology of the Chattahoochee in coastal plain sediments near Millers Pond, Burke County, River Valley, western Georgia and eastern Alabama, in Frey, Georgia, 1992-93: Georgia Geologic Survey Information Cir R.W., ed., Excursions in southeastern geology, v. 2: Geologi cular 96, 34 p., 1 pi. in pocket. cal Society of America, Annual Meeting (93rd), Atlanta, Clarke, J.S., and West, C.T., 1994, Development of water-table and 1980, Field Trip Guidebooks, p. 422-423. potentiometric-surface maps for coastal plain aquifers in the ———1980b, Paleogene sporomorphs from South Carolina and vicinity of the Savannah River Site, South Carolina and Geor quantitative correlations with the Gulf Coast: Palynology, v. gia [abs.]: Geological Society of America Abstracts with Pro 4, p. 125-179. grams, v. 26, no. 4, p. 8. ———1984, Lower Tertiary pollen biostratigraphy, Maryland and Edwards, L.E., 1992, Dinocysts from the lower Tertiary units in the Virginia, in Frederiksen, N.O., and Krafft, Kathleen, eds., Savannah River area, South Carolina and Georgia, in Zullo, Cretaceous and Tertiary stratigraphy, paleontology and struc V.A., Harris, W.B., and Price, Van, eds., Savannah River ture, southwestern Maryland and northeastern Virginia: region; Transition between the Gulf and Atlantic Coastal American Association of Stratigraphic Palynologists Field Plains: Proceedings of the Second Bald Head Island Confer Trip Volume and Guidebook, p. 163-168. ence on Coastal Plains Geology, Hilton Head Island, Novem ———1988, Sporomorph biostratigraphy, floral changes, and pale- ber 6-11, 1990, p. 97-99. oclimatology, Eocene and earliest Oligocene of the eastern Edwards, L.E., and Clarke, J.S., 1992, Biostratigraphic investiga Gulf Coast: U.S. Geological Survey Professional Paper 1448, tions help evaluation of the ground-water-flow system near 68 p. the Savannah River Site, Georgia and South Carolina [abs.], ———1991, Midway an (Paleocene) pollen correlations in the East in Proceedings, Fifth North American Paleontological Con ern United States: Micropaleontology, v. 37, p. 101-123. vention, Chicago, 111., June 28-July 1, 1992: Paleontological -1998, Upper Paleocene and lowermost Eocene angiosperm Society Special Publication 6, p. 90. pollen biostratigraphy of the eastern Gulf Coast and Virginia: Edwards, L.E., and Frederiksen, N.O., 1992, Paleogene palyno- Micropaleontology, v. 44, p. 45-68. morph correlations in eastern Georgia [abs.]: Geological Frederiksen, N.O., Bybell, L.M., Christopher, R.A., Crone, A.J., Society of America Abstracts with Programs, v. 24, no. 2, p. Edwards, L.E., Gibson, T.G., Hazel, J.E., Repetski, J.E., Russ, 14. D.P., Smith, C.C., and Ward, L.W., 1982, Biostratigraphy and Edwards, L.E., Frederiksen, N.O., Bybell, L.M., Gohn, G.S., Self- paleoecology of lower Paleozoic, Upper Cretaceous, and Trail, J.M., Gibson, T.G., Bukry, David, and Fleming, R.F., lower Tertiary rocks in U.S. Geological Survey New Madrid 1997, Mysteries solved in the stratigraphy of the updip coastal test wells, southeastern Missouri: Tulane Studies in Geology plain of Georgia [abs.]: Fifth Annual Clemson University and Paleontology, v. 17, p. 23^45. Hydrogeology Symposium, Abstracts, no pagination. Frederiksen, N.O., and Christopher, R.A., 1978, Taxonomy and Elsik, W.C., 1968a, Palynology of a Paleocene Rockdale lignite, biostratigraphy of Late Cretaceous and Paleogene triatriate Milam County, Texas. I. Morphology and taxonomy: Pollen pollen from South Carolina: Palynology, v. 2, p. 113-145. et Spores, v. 10, p. 263-314. Gellici, J.A., and Logan, W.R., 1993, Preliminary Stratigraphic and ———1968b, Palynology of a Paleocene Rockdale lignite, Milam hydrostratigraphic correlation of four deep coreholes east of County, Texas. II. Morphology and taxonomy (end): Pollen et the Savannah River Site in Allendale, Barnwell and Aiken Spores, v. 10, p. 599-664. Counties, South Carolina [abs.]: Geological Society of Amer -1974, Characteristic Eocene palynomorphs in the Gulf ica Abstracts with Programs, v. 25, no. 4, p. 17. Coast, U.S.A.: Palaeontographica, ser. B, v. 149, p. 90-111. Harris, M.K., Aadland, R.K., and Westbrook, T.M., 1992, Litho- Fairchild, W.W., and Elsik, W.C., 1969, Characteristic palyno logical and hydrological characteristics of the Tertiary morphs of the lower Tertiary in the Gulf Coast: Palaeonto hydrostratigraphic systems of the General Separations Area, graphica, ser. B, v. 128, p. 81-89. Savannah River Site, South Carolina, in Zullo, V.A., Harris, Falls, W.F., Baum, J.S., and Prowell, D.C., 1997, Physical stratig W.B., and Price, Van, eds., Savannah River region; Transition raphy and hydrostratigraphy of Upper Cretaceous and Pale between the Gulf and Atlantic Coastal Plains: Proceedings of ocene sediments, Burke and Screven Counties, Georgia: the Second Bald Head Island Conference on Coastal Plains Southeastern Geology, v. 36, p. 153-176. Geology, Hilton Head Island, November 6-11, 1990, p. 68- Falls, W.F., Prowell, D.C., Edwards, L.E., Frederiksen, N.O., Gib- 73. son, T.G., Bybell, L.M., and Gohn, G.S., 1993, Preliminary Jarzen, D.M., 1978, The terrestrial palynoflora from the Creta correlation of geologic units in three coreholes along the ceous-Tertiary transition, Alabama, U.S.A.: Pollen et Spores, Savannah River in Burke and Screven Counties, Georgia v. 20, p. 535-553. POLLEN BIOSTRATIGRAPHY OF LOWER TERTIARY SEDIMENTS FROM FIVE CORES, GEORGIA H21

Jones, E.L., 1962, Palynology of the Midway-Wilcox boundary in from Miller pit, Henry County, Tennessee: Palaeontograph- south-central Arkansas: Gulf Coast Association of Geological ica, ser. B, v. 157, p. 44-96. Societies Transactions, v. 12, p. 285-294. Prowell, D.C., Edwards, L.E., and Frederiksen, N.O., 1985 [1986], Krutzsch, W., 1970, Atlas der mittel- und jungtertiaren dispersen The Ellenton Formation in South Carolina—A revised age Sporen- und Pollen- sowie der Mikroplanktonformen des designation from Cretaceous to Paleocene, in Stratigraphic nordlichen Mitteleuropas, VII: Jena, VEB Gustav Fischer notes, 1984: U.S. Geological Survey Bulletin 1605-A, p. Verlag, 175 p. A63-A69. Leeth, D.C., Falls, W.F., Edwards, L.E., Frederiksen, N.O., and Stover, L.E., Elsik, W.C., and Fairchild, W.W., 1966, New genera Fleming, R.F., 1996, Geologic, hydrologic, and water-chemis and species of early Tertiary palynomorphs from Gulf Coast: try data for a multi-aquifer system in coastal plain sediments Kansas University Paleontological Contributions, Paper 5, 10 near Girard, Burke County, Georgia, 1992-95: Georgia Geo P- logic Survey Information Circular 100, 26 p., 1 pi. in pocket. Strom, R.N., Kaback, D.S., and Schramke, J.A., 1992, Groundwa- Lucas-Clark, Joyce, 1992, Problems in Cretaceous palynostratigra- ter geochemistry and flow path modeling, Savannah River phy (dinoflagellates and pollen) of the Savannah River Site Site, S.C. [abs.]: Geological Society of America Abstracts area, in Zullo, V.A., Harris, W.B., and Price, Van, eds., Savan with Programs, v. 24, no. 2, p. 69. nah River region; Transition between the Gulf and Atlantic Coastal Plains: Proceedings of the Second Bald Head Island Thomson, P.W., and Pflug, H.D., 1953, Pollen und Sporen des mit- Conference on Coastal Plains Geology, Hilton Head Island, teleuropaischen Tertiars: Palaeontographica, ser. B, v. 94, 138 November 6-11, 1990, p. 81-82. P- Nichols, D.J., 1973, North American and European species of Tschudy, R.H., 1973a, Stratigraphic distribution of significant Momipites ("Engelhardtia") and related genera: Geoscience Eocene palynomorphs of the Mississippi embayment: U.S. and Man, v. 7, p. 103-117. Geological Survey Professional Paper 743-B, 24 p. Nichols, D.J., and Traverse, Alfred, 1971, Palynology, petrology, ———1973b, Complexiopollis pollen lineage in Mississippi and depositional environments of some early Tertiary lignites embayment rocks: U.S. Geological Survey Professional Paper in Texas: Geoscience and Man, v. 3, p. 37-48. 743-C, 15 p. Potter, F.W., Jr., 1976, Investigations of angiosperms from the ———1975, Normapolles pollen from the Mississippi embayment: Eocene of southeastern North America—Pollen assemblages U.S. Geological Survey Professional Paper 865, 42 p.

~~PLATES 1, 2 PLATE 1~~

~~[All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. Sparganiaceaepollenites sp., Ellenton Formation, Girard core (521.0-521.2 ft), Burke County. 2. Milfordia hungarica (Kedves) Krutzsch & Vanhoorne in Krutzsch (1970), Congaree Formation, Thompson Oak core (192.0 ft). Burke County. 3. Milfordia incerta (Pflug & Thomson in Thomson and Pflug, 1953) Krutzsch, Ellenton Formation, Girard core (484.1^84.3 ft), Burke County. 4. Momipites tenuipohis group of Frederiksen and Christopher (1978), Snapp Formation, McBean core (264.0 ft). Burke County. 5. Momipites coryloides Wodehouse, Congaree Formation, Thompson Oak core (192.0 ft), Burke County. 6. Momipites dilatus Fairchild in Stover and others (1966), Ellenton Formation, Millhaven core (571.0 ft), Screven County. 7, 8. Platycarya platycaryoides (Roche) Frederiksen & Christopher, Congaree Formation, Millhaven core (490.0 ft), Screven County. Interference contrast. 9, 10. Platycarya sp. A of Frederiksen and Christopher (1978) (from drilling mud contamination), Steel Creek Formation (Cretaceous), Millhaven core (755.0-755.3 ft), Screven County. 11. Platycarya sp., Congaree Formation, Millhaven core (490.0 ft), Screven County. The specimen has several irregular pseudocolpi; interference contrast. 12. Platycarya sp. (from drilling mud contamination), Steel Creek Formation (Cretaceous), Millhaven core (755.0-755.3 ft), Screven County. 13. Platycarya sp., Fourmile Branch Formation, Girard core (415.2^15.5 ft), Burke County. 14. Momipites-PlicatopoHis-Platycaryapollenites complex of Frederiksen (1979), Congaree Formation, Millhaven core (490.0 ft), Screven County. 15. Plicatopollis triorbicularis type of Frederiksen and Christopher (1978), Snapp Formation. McBean core (264.0 ft). Burke County. 16. Ulmipollenites tricostatus (Anderson) Frederiksen, Ellenton Formation, Girard core (484.1-484.3 ft), Burke County. 17. Ulmipollenites krernpii (Anderson) Frederiksen, Ellenton Formation, Girard core (484.1-484.3 ft), Burke County. 18. Malvacipollis cf. M. tschudyi Frederiksen of Frederiksen (1988), Congaree Formation, Thompson Oak core (192.0 ft), Burke County. 19. Spinaepollis spinosus (Potonie) Krutzsch, Ellenton Formation, Millhaven core (579.5 ft), Screven County. 20. Eucommia type (tricolporate) of Frederiksen (1988), Congaree Formation, Thompson Oak core (192.0 ft), Burke County. 21, 22. Spinizonocolpites prominatus (Mclntyre) Stover & Evans, Santee Limestone, Thompson Oak core (174.0 ft), Burke County. 23. Aesculiidites circumstriatus (Fairchild in Stover and others, 1966) Elsik, Ellenton Formation, Thompson Oak core (281.0 ft), Burke County. 24. llexpollenites sp., Santee Limestone, McBean core (181.0 ft). Burke County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-H, PLATE 1

~~22 40 Jim ANGIOSPERM POLLEN GRAINS PLATE 2~~

~~[All specimens are from Screven and Burke Counties, Georgia]~~

Figure 1. Pseudoplicapollis limitatus Frederiksen, Ellenton Formation, Girard core (484.1- 484.3 ft), Burke County. 2, 3. Nudopollis lerminalis (Pflug & Thomson in Thomson and Pflug, 1953) Pflug, Ellenton Formation. 2, Girard core (532.5-532.7 ft), Burke County; 3, Thompson Oak core (281.0 ft), Burke County. 4. Pseudolaesopollis ventosus (Potonie) Frederiksen, Santee Limestone, McBean core (181.0ft), Burke County. 5. Choanopollenites sp. cf. C. consanguineus Tschudy of Frederiksen (1979), Ellenton Formation, Millhaven core (589.0 ft), Screven County. 6. Insulapollenites rugulatus Leffingwell, Snapp Formation, McBean core (264.0 ft), Burke County. 7. Intmtriporopollenites sp., Ellenton Formation, Millhaven core (581.0 ft), Screven County. 8. Pseudoplicapollis serenus Tschudy, Ellenton Formation, Millers Pond core (252.0- 257.0 ft), Burke County. 9. Osculapollisl colporatus Frederiksen, Ellenton Formation, Thompson Oak core (302.0 ft), Burke County. 10. Trudopollis plenus Tschudy, Ellenton Formation, Girard core (484.1^84.3 ft), Burke County. 11. Symplocos! sp. aff. Symplocosl sp. 1 of Frederiksen (1988), Santee Limestone, Millers Pond core (148.0 ft), Burke County. 12. Friedrichipollis sp., interference contrast. Ellenton Formation, Millhaven core (581.0 ft), Screven County. 13. Bombacacidites reticulatus Krutzsch, Ellenton Formation, Millers Pond core (252.0-257.0 ft). Burke County. 14. Bombacacidites nacimientoensis (Anderson) Elsik, Ellenton Formation, Millhaven core (571.0 ft), Screven County. 15. Lanagiopollis cribellatus (Srivastava) Frederiksen, Ellenton Formation, Millhaven core (581.0 ft), Screven County. 16. Lanagiopollis sp., probably L. hadrodictyusFredenksen, Congaree Formation, Thompson Oak core (183 ft), Burke County. U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-H. PLATE 2

~~J____I____I 0 20 40 Jim~~

~~ANGIOSPERM POLLEN GRAINS~~

~~U.S. Department of the Interior U.S. Geological Survey~~

~~Foraminifera from Paleogene Sediments from the Millhaven and Millers Pond Cores, Screven and Burke Counties, Georgia By Thomas G. Gibson~~

~~U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-1~~

~~Prepared in cooperation with the U.S. Department of Energy and the Georgia Geologic Survey~~

~~GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA~~

~~Edited by Lucy E. Edwards~~

~~CONTENTS~~

Abstract ...... II Introduction ...... 1 Acknowledgments ...... 2 Material and Methods ...... 2 Biostratigraphy ...... 2 Paleoenvironmental Analysis...... 4 MillhavenCore...... 5 Ellenton Formation ...... 5 Snapp Formation ...... 8 Congaree Formation ...... 8 Warley Hill Formation ...... 9 Santee Limestone ...... 10 Barnwell Unit ...... 10 Millers Pond Core...... 10 Santee Limestone ...... 11 Conclusions ...... 12 References Cited ...... 12

~~PLATE [Plate follows References Cited]~~

~~1. Nodogenerina, Pseudonodosaria, Globoconusa, Pyramidina, Pulsiphonina, Siphonina, Cibicides, and Pararotalia.~~

~~FIGURES~~

1. Index map showing the Savannah River Site and the location of the Millhaven and Millers Pond test holes in Screven and Burke Counties, Georgia...... 12 2. A lithologic log and paleobathymetry of the Millhaven core ...... 3 3. A lithologic log of the Millers Pond core...... 4

~~TABLES~~

~~1, 2. Sedimentary characteristics of foraminiferal samples from the— 1. Millhaven core...... 16 2. Millers Pond core ...... 11~~

GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, EASTERN GEORGIA Foraminifera from Paleogene Sediments from the Millhaven and Millers Pond Cores, Screven and Burke Counties, Georgia

~~By Thomas G. Gibson1~~

ABSTRACT environments during the deposition of most upper Pale ocene and Eocene beds, but an upper Paleocene dark clay interval contains assemblages suggestive of high-productiv Paleocene and Eocene foraminifers were studied for biostratigraphic and paleoenvironmental analysis in cores ity and low-oxygen environments. from two test holes in the eastern Georgia Coastal Plain. The Millhaven test hole, located southeast of the Millers Pond test hole, is in the more downbasin position. In the INTRODUCTION Millhaven core, foraminifers are present in lower and upper Paleocene strata of the Ellenton Formation, lower middle Paleogene foraminifers from the Millhaven and Millers Eocene strata of the Congaree and Warley Hill Formations, Pond cores were examined during a study of the hydrogeo- upper middle Eocene strata of the Santee Limestone, and logic framework of easternmost Georgia across the river upper Eocene and questionable lower Oligocene strata of from the Savannah River Site in South Carolina (fig. 1). the Barnwell unit. Foraminifers were recovered only from This study examined foraminiferal assemblages both for upper middle Eocene strata of the Santee Limestone in the biostratigraphic placement of the strata and for interpreta Millers Pond core. The Millers Pond site is the more west tion of depositional environments. Foraminiferal assem erly of the two sites and is in a more upbasin position. blages are discussed in a sample-by-sample format to Foraminifers are moderately to highly altered diagenet- provide the maximum amount of information from this area ically in many of the sandy or carbonate-rich intervals in where little foraminiferal information is currently available. these cores, and the alteration makes specific identifications difficult. Diagnostic planktonic species are found only in In the more easterly, and thus downbasin, Millhaven beds of early Paleocene age. Some benthic foraminiferal core, foraminifers are found both in Paleocene and Eocene species that have restricted regional biostratigraphic ranges strata. The specimens are well preserved in the more clayey are present. These species suggest placements for some strata, but most are highly altered in the more sandy and strata in the early part of the late Paleocene and in the mid limy beds. In the more upbasin Millers Pond core, foramini dle Eocene. fers are found only in the Santee Limestone of late middle Foraminiferal assemblages suggest that most upper Eocene age. These specimens occur in carbonate-rich, Paleocene and Eocene beds were deposited in shal sandy sediments, and their tests are moderately to highly low-marine environments with water depths of less than altered diagenetically. 100 ft. Assemblages in a few intervals, however, suggest Some common and important stratigraphic marker somewhat deeper inner-middle to middle neritic environ benthic species and one stratigraphically important plank- ments. Foraminiferal assemblages suggest well-oxygenated tonic species are illustrated by scanning electron micro scope (SEM) photographs (pi. 1). A high degree of Retired from the U.S. Geological Survey. Present address: Depart recrystallization within many assemblages, however, makes ment of Paleobiology. National Museum of Natural History, Smithsonian it difficult to obtain satisfactory pictures of many species, Institution, Washington, DC 20560-0121. particularly those from the middle Eocene. 12 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

82° 30' 82 c 81° 30' particles adhering to the specimens, chamber infillings, cal careous overgrowths, or heavy recrystallization of the test wall. In these samples, the foraminifers were picked from the entire sediment residue that remained after washing. The degree of diagenetic alteration of the foraminifers in many samples makes it difficult to identify these speci 33° 30' mens to the species level. In addition, diagenetic alteration may have selectively removed certain taxa from the original foraminiferal assemblage. Because of these possible biases, /' samples were studied on a qualitative (species present or /' / - -\ / ° absent) basis only. '\ Jefferson - In the Millhaven core, 23 samples from 5 Paleocene 33° - ^"\ i and Eocene units contained foraminifers (fig. 2). In the Millers Pond core, only three samples from the Santee Limestone contained foraminifers (fig. 3). Sample depths are recorded to the nearest 0.5 ft, except in the lower part of the Millhaven core where sample depths are recorded to the nearest 0.1 ft. 0 10 20 30 KILOMETERS Illustrated specimens, other study specimens, faunal 32° 30' slides, and foraminiferal concentrates are deposited in the Cushman Foraminiferal Collection at the U.S. National EXPLANATION Museum of Natural History (USNM), Smithsonian Institu Millhaven • Test hole site and informal name of site tion, Washington, D.C.

Figure 1. Index map showing the Savannah River Site and the BIOSTRATIGRAPHY location of the Millhaven and Millers Pond test holes in Screven and Burke Counties, Georgia. Gohn (1988) summarized the early Cenozoic geology of the southern Atlantic Coastal Plain. This work contains ACKNOWLEDGMENTS numerous references to the lithostratigraphy of Paleogene deposits in Georgia and South Carolina. Relatively few pub Thomas Servais (U.S. Geological Survey) prepared the lications, however, exist on the biostratigraphy of Paleogene foraminiferal samples and aided in the sediment descrip Foraminifera in Georgia and South Carolina, and even fewer tions. Jean M. Self-Trail and Amanda Chapman (U.S. Geo contain illustrations of the species. Herrick (1961) summa logical Survey) prepared the illustrations. Raymond A. rized the occurrence of many benthic species in subsurface Christopher (Clemson University) and Harry J. Dowsett samples from Paleogene formations of Georgia, but the spe (U.S. Geological Survey) made helpful suggestions on the cies were not illustrated. manuscript. Biostratigraphic ranges of many benthic foraminiferal taxa occurring in Georgia and South Carolina deposits largely are undocumented, both in terms of their ranges in MATERIAL AND METHODS Paleogene deposits of the Southeastern United States and in terms of the intercontinental biostratigraphic zonations. I Foraminifers were prepared from core sections several compared the benthic species, when possible, with their bio inches in length. The outside rind of each core segment, stratigraphic distribution in neighboring areas to the north in which may contain contaminated drilling mud, was North Carolina (Copeland, 1964; Jones, 1983) and Virginia removed before processing. Core sections were washed over and Maryland (Nogan, 1964; Gibson and others, 1980; a 63-micrometer screen that retained all sand-sized and Poag, 1989), and to the southwest in Alabama (Bandy, coarser particles. 1949), where more detailed studies of these faunas have We then followed two procedures depending upon the been made. Even in these areas, however, the ranges of state of foraminiferal preservation. In samples containing benthic species in terms of intercontinental biostratigraphic well-preserved foraminiferal assemblages, the specimens zonations are largely unknown at the present time. were concentrated from other sand-sized sedimentary parti Planktonic foraminifers can be widely distributed in cles by soap flotation. However, in many samples, the fora- the oceans and, therefore, are widely used in minifers were altered diagenetically and exhibited one or intercontinental correlation and zonations. Unfortunately, more of the following conditions: extraneous sedimentary they are quite rare in Paleogene strata in the two studied FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 13

~~EXPLANATION~~

~~Fossils~~

~~Calcareous sand~~

~~Clay~~

~~Clayey sand~~

~~Sand~~

~~Sandy limestone~~

~~Limestone~~

~~Clayey limestone i- i -i~~

~~Calcareous clay~~

~~Foraminiferal sample~~

~~? Uncertain age~~

~~600 m -^-=--=.~~

~~642~~

Figure 2. A lithologic log and paleobathymetry of the Millhaven core. The solid triangles indicate the locations of the productive foraminiferal samples. A nonproductive sample from 219 ft is not shown. The calcareous nannofossil zones are from Bybell (this volume, chap. F). 14 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~O I ^ 0 LITHOLOGY ob SERIES LU1 ^1 Q s§ o- 0~~

o EXPLANATION Barnwell Q. Q. unit => Eocene :.- • . Massive t clay 100- I I •a0 Santee •o » | | Laminated Limestone ^ clay > I I Congarfifi Formation — — Sand —— —— Snapp £s_ 200- 0 a. Formation Paleocene Q. => Limestone Ellenton 7P Formation o Foraminiferal sample

Figure 3. A lithologic log of the Millers Pond core. The solid triangles indicate the locations of the foraminiferal samples. The lithology is from Clarke and others (1994) and the lithostratigraphy is from Falls and Prowell (this volume, chap. A). cores. The few planktonic specimens recovered from most PALEOENVIRONMENTAL ANALYSIS samples consist mainly of juvenile individuals, which are difficult to place in a specific taxon. The rarity of adult The paleoenvironmental analysis is largely based on planktonic specimens in the deposits is due primarily to the two approaches: (1) the specific and generic composition of shallow-water depositional environments of the preserved the benthic foraminiferal assemblage and (2) the population Paleogene strata in this area. The natural rarity of planktonic characteristics of the entire foraminiferal assemblage. Most specimens in these environments may be augmented by the benthic species occurring in Paleogene assemblages became extensive diagenetic history of many of the samples. Tests extinct during the early and middle Cenozoic. Therefore, for of planktonic species are more vulnerable to dissolution Paleogene species, data on environmental tolerances and during diagenesis than are tests of most benthic species distribution in modern environments usually is not possible. (Murray, 1991). Much less is known biostratigraphically However, general paleoenvironmental limits on some about benthic foraminifers, and they are more closely extinct species were suggested in studies of Paleogene subjected to environmental controls. Yet, benthic assemblages in adjacent areas such as those of Olsson and foraminifers compose more than 95 percent of most Wise (1987) in New Jersey and Poag (1989) in Virginia. assemblages. Numerous benthic genera, however, range from the Paleogene into modern faunas. Although benthic foramin Most age assignments of strata used in this paper result iferal genera usually have wider environmental tolerances from the calcareous nannofossil study of these cores by than any single contained species, some benthic genera have Bybell (this volume, chap. F). Bybell and I have found in relatively restricted environmental tolerances for all their studies of Paleogene strata in other parts of the Eastern and modern species. The occurrences of fossil species within Southeastern United States that diagnostic calcareous nan these genera also seem to mirror similar environmental con nofossil species are much more common in shallow-water trols. Generalized environmental interpretations regarding deposits than are diagnostic planktonic foraminiferal spe depth, productivity, and oxidation levels were reconstructed cies (Gibson and Bybell, 1995). In the Millhaven core, from these genera wherever possible. planktonic foraminifers, in conjunction with calcareous Population characteristics of the entire foraminiferal nannofossils, were valuable in a more accurate placement of assemblage that can be used for paleoenvironmental analy the upper lower Paleocene strata. sis include benthic species diversity and the planktonic/ FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 15 benthic ratio. Gibson and Buzas (1973) conducted studies The nine samples examined from the higher part of the on species diversity, and Gibson (1988, 1989) studied plank- Ellenton Formation (631.3-581 ft) are of early late tonic/benthic ratios. Both sets of studies show that patterns Paleocene age (calcareous nannofossil Zone NP 5) of these assemblage characteristics found with increasing according to Bybell (this volume, chap. F). Some benthic water depth are similar between the early and middle Ceno- foraminiferal species, such as Cibicides compressus Olsson, zoic faunas of the Atlantic and eastern Gulf Coastal Plains that occur in these samples have their highest occurrences in and the modern faunas of the western Atlantic Ocean and Virginia and Maryland in strata placed in Zone NP 5 the Gulf of Mexico. (Nogan, 1964; Bybell and Gibson, 1991), which supports this age assignment. Five intervals with differing foraminiferal assemblages MILLHAVEN CORE are present in the formation: (1) a highly altered, low-diver sity assemblage of early Paleocene age at 636.8 ft; (2) an The Millhaven test hole (33X048) site, lat 32°53'25" assemblage containing apparent mixing of specimens from N., long 81°35'43" W., is located in Screven County, Ga. lower Paleocene beds with early late Paleocene specimens (fig. 1). Land surface elevation of the drill site is 110 ft. at 631.3 ft; (3) an assemblage suggesting normal productiv Twenty-four samples between the depths of 637 and 118 ft ity and oxygen levels with a probable water depth range of were examined for foraminifers (table 1, fig. 2). Foramini- 100 to 200 ft, which occurs at 628.7 ft in clayey glauconitic fers are present in both lower and upper Paleocene strata of sand; (4) an assemblage suggestive of water depths of less the Ellenton Formation, lower middle Eocene strata of the than 100 ft but having high-productivity and (or) low-oxy Congaree and Warley Hill Formations, upper middle gen conditions, which occurs in dark clay samples from Eocene strata of the Santee Limestone, and upper Eocene 621.2 to 599.1 ft; and (5) an assemblage suggestive of water and possibly lower Oligocene strata of the Barn well unit in depths of less than 100 ft with normal marine oxygen condi the Millhaven core. tions in samples from 593.7 to 581 ft, which occurs in cal careous and clayey sand beds. ELLENTON FORMATION 636.8ft (early Paleocene).—The sample from 636.8 ft contains relatively few specimens of a low-diversity assem The lower beds of the Ellenton Formation in the Mill- blage of highly corroded foraminifers, most of which have haven core, as seen in the lowest foraminiferal sample stud calcite rhombohedrons attached to their tests. The poor ied at 636.8 ft, contain a more highly altered and a lower preservation precludes definitive identifications of some diversity benthic assemblage than the nine samples studied specimens beyond the generic level. from the middle and upper parts of the formation (631.3 to Cibicides compressus Olsson, Bulimina sp., Cibicides 581 ft). The lowest sample is of early Paleocene age (lower sp., and Gyroidina sp. are present in the benthic foramin part of calcareous nannofossil Zone NP 4) as discussed iferal assemblage. Cibicides compressus Olsson occurs in below, and the nine higher samples are of early late Pale both lower and lower upper Paleocene strata in Virginia and ocene age (calcareous nannofossil Zone NP 5) (Bybell, this Maryland (Nogan, 1964; Thomas Gibson, unpub. data). The volume, chap. F). highly altered specimens and the few species present in the Lower Paleocene beds in the Millhaven core have a assemblage suggest that much of the original assemblage thickness of approximately 10 ft or less. These beds appar was removed during diagenesis. Extensive diagenesis could ently represent a relatively thin remnant of a formerly much be expected as this sample is near the top of the lower Pale thicker lower Paleocene deposit in this area that underwent ocene beds. There is a disconformity between lower Pale significant erosional removal during the latest early and ear ocene and lower upper Paleocene strata located somewhere liest late Paleocene. Several of the highest Cenozoic sea lev between this sample and the overlying sample at 631.3 ft. els occurred in the early Paleocene (Haq and others, 1987), Subaerial exposure of these beds was likely during the for and deposits representing these extensive seas are found in mation of the disconformity. many areas in the Atlantic Coastal Plain. Studies on Paleo- The foraminiferal assemblage also contains recogniz gene deposits of western Georgia and eastern Alabama able specimens of the important planktonic species Glob- (Gibson, 1992) and Maryland (Gibson and Bybell, 1994) oconusa daubjergensis (Bronnimann). This planktonic found that these lower Paleocene deposits represented the species ranges through much of the early Paleocene (plank deepest water deposition and the highest sea levels of any tonic foraminiferal Zone PI, Danian) but does not range Paleogene unit that is found in those areas. However, the into the latest early Paleocene (Toumarkine and Luter- lower Paleocene middle to outer neritic deposits are very bacher, 1985; Berggren and others, 1995). Bybell (this vol patchy in their present-day occurrence in the Atlantic ume, chap. F), on the basis of the calcareous nannofossils, Coastal Plain, which suggests that widespread erosion of places this sample interval into calcareous nannofossil Zone these deposits occurred during latest early Paleocene, late NP 4, which is of latest early Paleocene and earliest late Paleocene, and younger times. Paleocene age (Berggren and others, 1995). The presence of 16 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

~~Table 1. Sedimentary characteristics of foraminiferal samples from the Millhaven core.~~

~~Sample depth _ ,. , Sedimentary characteristics~~

Barnwell unit 118 ———— Calcareous sand; 71 percent sand size by weight; sand fraction consists of abundant recrystallized shell fragments and bryozoan fragments with about 10 percent quartz; trace of glauconite. 219 ———— Calcareous quartz silty sand; 87 percent sand size by weight; sand fraction consists of 70 percent quartz, 20 percent calcareous grains, and 10 percent shell fragments. Santee Limestone 248 ———— Calcareous sand; 73 percent sand size by weight; sand fraction consists of 85 percent carbonate and 15 percent glauconite; just traces of shell debris and quartz. 307 ———— Limestone with some recrystallized shell fragments and a trace of pyrite. 346 ———— Calcareous unit with trace of glauconite. 355 ———— Calcareous unit with traces of quartz and glauconite. 365 ———— Calcareous unit with 15 percent glauconite. Warley Hill Formation 404 ———— Calcareous quartz sand; 85 percent sand size by weight; sand fraction consists of 45 percent carbonate, 30 percent quartz, and 25 percent shell fragments. 413 ———— Calcareous quartz sand; 84 percent sand size by weight; sand fraction consists of 55 percent quartz, 40 percent car bonate, and 5 percent glauconite. 426.5 ——— Calcareous unit with 10 percent glauconite and 5 percent pyrite, trace of quartz. 456 ———— Calcareous unit with 20 percent glauconite, 10 percent shell hash, and 5 percent quartz. Congaree Formation 473.5 ——— Quartz sand, 88 percent sand size by weight; sand fraction consists of 60 percent quartz and 40 percent glauconite. 481.5 ——— Quartz sand, 90 percent sand size by weight; sand fraction consists of 55 percent quartz and 45 percent glauconite. 495.5 ——— Quartz sand, 95 percent sand size by weight; sand fraction consists of 85 percent quartz and 15 percent glauconite with a trace of phosphate. Ellenton Formation 581 ———— Calcareous unit with 20 percent shell fragments and 10 percent quartz. 589 ———— Calcareous unit with 15 percent shell fragments. 593.7 ——— Clayey very fine sand, discontinuous clay laminae, very shelly including small oyster. [At 595.2 ft, there appears to be burrowed contact of sand into underlying clay] 599.1 ——— Dark clay, thin discontinuous sand lenses, highly bioturbated, small clam shells. 609.8 ——— Dark clay, thin discontinuous sand lenses, highly bioturbated. 613.1 ——— Dark clay, thin discontinuous sand lenses, highly bioturbated. 621.2 ——— Dark clay, thin discontinuous sand lenses, highly bioturbated. [At 622.4 ft, there is a rapid downward change with no noticeable break from clay to quite glauconitic medium sand, mostly slightly indurated; this change occurs with a gradual downward decrease in the amount of clay over the upper 2 ft to considerably lower levels] 628.7 ——— Clayey glauconitic fine to medium sand with the more sandy intervals being somewhat indurated. 631.3 ——— Clayey glauconitic fine to medium sand. 636.8 ——— Clayey glauconitic fine to coarse sand.

The Snapp Formation was cored above the Ellenton Formation from 570 to 504 ft in the Millhaven core; no foraminifers were observed and no samples were taken. FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 17

G. daubjergensis (Bronnimann) indicates that this interval transgressive beds of the lower upper Paleocene more likely belongs to the older, or early Paleocene, part of calcareous than either of two other interpretations for the age disparity. nannofossil Zone NP 4 (Berggren and others, 1995). These basal transgressive beds contain calcareous The probable diagenetic removal of much of the nannofossils indicative of Zone NP 5. One other inter assemblage makes a meaningful paleoenvironmental pretation for the age disparity is downhole contamination of interpretation of the sample difficult. However, the moderate early late Paleocene calcareous nannofossils into lower abundance of the more dissolution susceptible planktonic Paleocene strata. Another is an unrecognized disconformity specimens suggests that planktonic specimens were that could have separated the foraminiferal and nannofossil abundant and that this sample reflects a relatively offshore samples taken from the core segment from 631.3-631.6 ft environment. (whether the two samples were taken from opposite ends of 631.3ft (late Paleocene with mixing of early Paleocene this core segment or both from the same end is unknown specimens).—The sample from 631.3 ft contains shal and undeterminable). low-marine benthic foraminiferal species that are similar to 628.7ft (late Paleocene).—-The sample from 628.7 ft those found in Paleocene strata to the north. Benthic taxa contains a well-preserved and diverse benthic assemblage. present include Lenticulina, Hanzawaia, Cibicides com- Benthic taxa include Hanzawaia, Cibicides compressus Ols pressus Olsson, Cibicides neelyi Jennings, Cibicides sp., son, Lenticulina, Alabamina, Pulsiphonina prima (Plum Pulsiphonina prima (Plummer), Gyroidina, Alabamina, and mer), Eponides lotus (Schwager), Nodosaria latejugata Nodosaria latejugata carolinensis Cushman. These taxa carolinensis Cushman, Pseudonodosaria tenuistriata occur both in lower and lower upper Paleocene strata in (Franke), Spiroplectammina wilcoxensis Cushman and Pon North Carolina, Virginia, and Maryland (Nogan, 1964; Gib- ton, Loxostomum, Nodogenerina plummerae (Cushman), son and others, 1980, Thomas Gibson, unpub. data). Epistominella minuta (Olsson), Bolivinopsis emmendorferi The calcareous nannofossil assemblage occurring in (Jennings), Pararotalia perclara (Loeblich and Tappan), and this sample suggests placement in Zone NP 5 of the lower Pyramidina virginiana (Cushman). This assemblage is char upper Paleocene (Bybell, this volume, chap. F). However, acteristic of the lowermost part of the Aquia Formation in this sample also contains moderately abundant lower Pale Virginia and Maryland (Nogan, 1964; Thomas Gibson, ocene planktonic foraminifers including Globoconusa unpub. data). Some of these species also range into the mid daubjergensis (Bronnimann) and Morozovella pseudobul- dle part of the Aquia Formation. The lowermost beds of the loides (Plummer). The presence of a calcareous nannofossil Aquia Formation are placed in calcareous nannoplankton assemblage that is indicative of an early late Paleocene age Zone NP 5 of the lower upper Paleocene; the middle beds suggests that the early Paleocene planktonic foraminifers in extend from Zone NP 6 to NP 8 (Gibson and others, 1991). this sample have been reworked from underlying lower Planktonic specimens make up a small proportion of the Paleocene deposits. The reworking of early Paleocene assemblage. The foraminiferal assemblage suggests shal planktonic foraminifers into lower upper Paleocene beds low-marine environments having water depths less than 200 placed in Zone NP 5 is seen in other localities in the Atlan ft, but possibly in the 100-ft or slightly deeper range. Nor tic Coastal Plain (Thomas Gibson, unpub. data). As dis mal marine productivity and oxygen levels were present. cussed above, much of the lower Paleocene material appears 621.2 ft (late Paleocene).—The sample from 621.2 ft to have been removed through erosion from the Millhaven contains a well-preserved and moderately diverse assem test hole site. blage that differs considerably from the underlying assem Relatively deep water depositional environments are blages. Benthic taxa include Epistominella minuta (Olsson), present during some intervals of Zones NP 3 and NP 4 of Fursenkoina, Pararotalia perclara (Loeblich and Tappan), the early Paleocene. Foraminiferal assemblages from these Pulsiphonina prima (Plummer), and Pyramidina virginiana intervals in the Atlantic Coastal Plain deposits thus contain (Cushman). Pararotalia perclara (Loeblich and Tappan) is abundant planktonic specimens, mostly composed of G. commonly found in Paleocene strata, but it is not found in daubjergensis (Bronnimann) and M. pseudobulloides beds younger than those placed in calcareous nannofossil (Plummer) (Thomas Gibson and Laurel Bybell, unpub. Zone NP 8 in Virginia and Maryland (Thomas Gibson, data). The abundant planktonic specimens apparently are unpub. data). The assemblage suggests shallow-marine reworked from these lower Paleocene deposits and incorpo environments having water depths around 100 ft or shal rated into the lower part of the strata that formed during the lower. The above-noted species dominate the assemblage. widespread marine transgression of Zone NP 5 in the early Their abundance suggests high-productivity and (or) late Paleocene. The exact location in the Millhaven core of low-oxygen depositional environments for the interval con the disconformable contact between the two different age taining this sample and the three overlying ones. This is in units within the Ellenton is uncertain, but apparently occurs contrast to the relatively normally oxygenated environments somewhere between 636.8 and 631.3 ft. that are characteristic of samples below 621.2 ft. The For the Millhaven core, I consider a similar reworking high-productivity and (or) low-oxygen assemblages occur in of lower Paleocene planktonic foraminifers into basal a dark clay interval, which contrasts with the underlying 18 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA interval of clayey, glauconitic, fine to medium sand. The (Cushman). The assemblage is characteristic of shal dark color of the clay also supports the idea that low-oxygen low-marine environments of less than 100-ft water depth. environments were present that would lead to increased 581 ft (late Paleocene).—The small benthic assem preservation of organic matter in the sediments. blage from 581 ft consists of moderately well preserved to 613.1 ft (late Paleocene).—The well-preserved assem partially recrystallized specimens. The low-diversity assem blage from 613.1 ft contains a relatively low diversity blage is dominated by Anomalinoides umboniferus (Schwa benthic component with few planktonic specimens. The ger) with lesser numbers of Pyramidina virginiana benthic assemblage is dominated by Pararotalia perclara (Cushman), compositionally similar to the two underlying (Loeblich and Tappan) and Fursenkoina, with lesser propor samples. However, the proportion of Pararotalia perclara tions of Epistominella minuta (Olsson), Pulsiphonina prima (Loeblich and Tappan) is considerably higher than found in (Plummer), and Pyramidina virginiana (Cushman). This the underlying samples. The increase in P. perclara (Loe benthic assemblage is similar to that of the underlying sam blich and Tappan) in this sample possibly signifies that ple. These species are either characteristic of, or found in, somewhat higher productivity and (or) lower oxygen levels high-productivity or low-oxygen environments (Poag, 1989; were present. Gibson and others, 1993; Thomas Gibson, unpub. data). 609.8 ft (late Paleocene).—The benthic assemblage from 609.8 ft is well preserved but shows relatively low spe SNAPP FORMATION cies diversity. The composition is similar to the two under The Snapp Formation was cored above the Ellenton lying assemblages, with Pararotalia perclara (Loeblich and Formation from 570 to 504 ft in the Millhaven test hole. No Tappan) and Fursenkoina being dominant. foraminifers were observed and no samples were taken. 599.1 ft (late Paleocene).—The well-preserved benthic assemblage from 599.1 ft has relatively low species diver sity and is highly dominated by Pararotalia perclara (Loe CONGAREE FORMATION blich and Tappan). Other abundant species include Epistominella minuta (Olsson), Fursenkoina, and Pyramid Three samples of the Congaree Formation from the ina virginiana (Cushman). The assemblage is similar to Millhaven test hole were examined; they came from those of the underlying three samples and suggests shal between depths of 495.5 and 473.5 ft. Benthic foraminiferal low-marine environments of about 100-ft water depth or species characteristic of middle Eocene strata in the South less with high-productivity and (or) low-oxygen conditions. eastern United States, such as Cibicides westi Howe, Burrowed contact.—At 595.2 ft, there appears to be a Siphonina claibornensis Cushman, Cancris involutus Cope- burrowed contact of overlying clayey very fine sand into the land, and Guembelitria columbriana Howe occur in these dark clay unit. The foraminiferal assemblages above and samples. Bybell (this volume, chap. F) placed these Conga below this surface differ considerably. ree samples in calcareous nannofossil Zone NP 14 (earliest 593.7 ft (late Paleocene).—'The sample from 593.7 ft middle Eocene). contains a low-diversity benthic assemblage consisting of Foraminiferal assemblages in the lower and upper moderately well preserved to slightly recrystallized speci Congaree samples suggest shallow-marine environments mens, and it also contains a few planktonic specimens. The with water depths of approximately 100 ft. However, a con assemblage is highly dominated by Anomalinoides umbon- siderably deeper water pulse with water depths of around iferus (Schwager) and also contains Cibicides alleni (Plum 300 ft is suggested by the assemblage in the middle sample mer), Gyroidinoides, Pyramidina virginiana (Cushman), at 481.5 ft. and Buliminella elegantissima (d'Orbigny). These species The Congaree samples, which are placed in calcareous commonly occur in upper Paleocene deposits, but most of nannofossil Zone NP 14 by Bybell (this volume, chap. F), them also occur in lower Eocene and younger strata. The contain much greater amounts of sand-sized particles assemblage is characteristic of shallow-marine environ (mostly very fine to fine grained, with both quartz and glau- ments having water depths less than 100 ft. The assemblage conite being abundant) (table 1), than do the calcareous differs from those in the underlying four samples by the samples from the overlying Warley Hill Formation. presence of A. umboniferus and C. alleni, which are charac 495.5 ft (middle Eocene).—The sample from 495.5 ft teristic of more oxygenated waters. This change suggests contains a moderately well preserved, moderately diverse that the burrowed surface at 595.2 ft separates two differing benthic assemblage that contains a few adult planktonic depositional settings. specimens. The most common or diagnostic benthic taxa are 589 ft (late Paleocene).—The small benthic assem Cibicides westi Howe, Cibicides sp., Gyroidinoides, Siphon- blage from 589 ft consists of moderately well preserved to ma claibornensis Cushman, Eponides lotus (Schwager), and partially recrystallized specimens. The low-diversity assem Anomalinoides umboniferus (Schwager). Siphonina clai blage is highly dominated by Anomalinoides umboniferus bornensis Cushman has its initial appearance in the South (Schwager) with lesser numbers of Pyramidina virginiana eastern United States in strata placed in calcareous FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 19 nannofossil Zone NP 13 of the late early Eocene. This spe these samples. Bybell (this volume, chap. F) placed the cies survives into the late Eocene (Thomas Gibson, unpub. Warley Hill in Zone NP 15 (early middle Eocene). data). The joint occurrence of this species and C. westi Foraminiferal assemblages in most of these samples Howe, which is characteristic of the middle Eocene, sug suggest shallow-marine environments with water depths of gests a middle Eocene age for the sample. The assemblage approximately 100 ft with even shallower depths for the suggests fairly shallow marine environments having water uppermost sample. depths of approximately 100 ft. The Warley Hill samples from 413 and 404 ft are cal 481.5 ft (middle Eocene).—-The sample from 481.5 ft careous quartz sands, but they contain much more carbonate contains a moderately well preserved and moderately matrix and carbonate sand grains, less glauconite and diverse benthic assemblage, and it also contains a moderate quartz, and somewhat coarser sand grains than do samples number of planktonic specimens. Benthic taxa include in the quartz sand of the Congaree Formation. Shell frag Gyroidina, Siphonina claibornensis Cushman, Cibicides ments are present in large amounts in the uppermost sample westi Howe, Cibicides alleni (Plummer), Cibicidoides sp., at 404 ft, which supports the interpretation of very shallow Cancris involutus Copeland, Eponides lotus (Schwager), marine environments for this interval. Trifarina, Bulimina, Bolivina, and Guembelitria columbi- 456 ft (middle Eocene).—The specimens in the sample ana Howe. Pseudohastigerina micro. (Cole) and Acarinina from 456 ft range from moderately well preserved to spp. compose the planktonic component. The presence of slightly recrystallized. Benthic species diversity is moder Cibicides westi Howe, Cancris involutus Copeland (which ate, and there are some planktonic specimens. Benthic spe occurs in middle Eocene beds in North Carolina, Jones, cies found include Valvulineria involuta Cushman and 1983), and Guembelitria columbiana Howe indicates a mid Dusenbury, Eponides carolinensis Cushman, Eponides lotus dle Eocene age. The composition of the benthic assemblage (Schwager), Cibicides westi Howe, Gyroidinoides octocam- and the relative abundance and diversity of planktonic spec eratus (Cushman and Hanna), Hanzawaia, and Caucasina. imens, including the presence of common adult forms, sug These benthic taxa place this sample in the middle Eocene. gest deposition in middle neritic environments with water The depositional environment had water depths around 100 depths of approximately 300 ft. This interpreted depth is ft or slightly deeper. significantly greater than that proposed for the underlying 426.5 ft (middle Eocene).—The foraminifers in the sample. This projected depth increase is accompanied by an sample from 426.5 ft are moderately well preserved. The increase in glauconite content to 45 percent of the sand frac assemblage has a moderately low species diversity and con tion from 15 percent in the lower sample. tains a moderately low number of planktonic specimens. Important benthic taxa include Gyroidinoides octocamera- 473.5 ft (middle Eocene).—Most specimens in the tus (Cushman and Hanna), Cibicides westi Howe, Eponides sample from 473.5 ft are recrystallized to a lesser or greater lotus (Schwager), Guembelitria columbiana Howe, and degree. The species diversity of the benthic assemblage is Caucasina. The benthic species suggest a middle Eocene moderately low, and some planktonic specimens are age. The assemblage suggests deposition in water depths of present. Important benthic taxa include Cibicides westi approximately 100 ft or slightly deeper. Howe, Eponides lotus (Schwager), Eponides carolinensis 413ft (middle Eocene).—The sample from 413 ft con Cushman, Bulimina, Bolivina, Lenticulina, and Valvulineria tains a moderately diverse benthic assemblage in which involuta Cushman and Dusenbury. The benthic assemblage, most specimens are slightly recrystallized. A few planktonic plus the occurrence of the planktonic species specimens are present. Important benthic taxa present in the Pseudohastigerina micra (Cole), places this sample in the sample include Gyroidinoides octocameratus (Cushman and middle Eocene. The assemblage suggests deposition in Hanna), Cancris involutus Copeland, Cibicides westi Howe, water depths of approximately 100 ft or slightly deeper, Valvulineria involuta Cushman and Dusenbury, Eponides which represents a considerable shallowing from the lotus (Schwager), and Guembelitria columbiana Howe. underlying sample. Glauconite remains an important These benthic species indicate a middle Eocene age for the constituent in the sample, but it is less abundant than in the sample. The assemblage suggests a depositional environ underlying sample. ment with water depths of approximately 100 ft. 404 ft (middle Eocene).—Most foraminifers in the sample from 404 ft are slightly recrystallized. The species WARLEY HILL FORMATION diversity is moderately low. The benthic assemblage con tains Cibicides westi Howe, Cibicides sp., Gyroidinoides Four Warley Hill samples were examined between octocamerata (Cushman and Hanna), Valvulineria involuta depths of 456 and 404 ft in the Millhaven core. Benthic for- Cushman and Dusenbury, Eponides carolinensis Cushman, aminiferal species that are characteristic of middle Eocene Eponides ouachitaensis Howe and Wallace, and Textularia. strata in the Southeastern United States, such as Cibicides There are only a few planktonic specimens. The presence of westi Howe and Guembelitria columbiana Howe, occur in C. westi Howe and other benthic species indicates a middle no GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA

Eocene age. The assemblage suggests warm, shal present. This assemblage, as well as the underlying two, low-marine waters, probably within the shallower part of a suggests water depths between 100 to 200 ft, which are 0- to 100-ft depth range. slightly deeper than any interpreted for age-equivalent strata in the limited number of samples from the Millers Pond core. SANTEE LIMESTONE 307 ft (late middle Eocene).—Only a few highly recrystallized foraminifers are present in the sample from Five samples were examined from the Santee Lime 307 ft. Identifiable benthic taxa include Cibicides westi, stone, between the depths of 365 and 248 ft in the Millhaven Cibicides sp., Cibicidoides sp., Elphidium, and Nonion. The core; all samples are placed by Bybell (this volume, chap. F) identifiable assemblage suggests shallow waters with depths in calcareous nannofossil Zone NP 17 (upper middle of 0 to 100 ft. Eocene). Most of these samples contain Cibicides westi 248 ft (late middle Eocene).—A few highly recrystal Howe and Siphonina claibornensis Cushman; the co-occur lized foraminifer specimens are present in the sample from rence of these benthic species is characteristic of middle 248 ft. Cibicides and Quinqueloculina are the most abun Eocene strata in the Southeastern United States. dant genera. No planktonic specimens or any age-diagnostic The lower three samples are from soft calcareous beds benthic taxa were recognized. The preserved assemblage and contain a slightly recrystallized but diverse foramin- suggests warm-water environments with depths of probably iferal fauna that suggests water depths of 100 to 200 ft. For- less than 100 ft. aminifers in the upper two samples (limestone and calcareous sand) are highly recrystallized; the relatively few recognizable specimens suggest possibly slightly shallower BARNWELL UNIT water depths of 100 ft or less. The lower sample examined from the Barnwell unit at 365 ft (late middle Eocene).—Most foraminifers in the 219 ft in the Millhaven core did not contain foraminifers. sample from 365 ft are slightly recrystallized. A diverse The upper sample examined from the Barnwell unit is con benthic assemblage is present, including Pseudononion, sidered either latest Eocene or earliest Oligocene in age Cibicides westi Howe, Cibicides sp., Siphonina claibornen (Bybell, this volume, chap. F). sis Cushman, Gyroidinoides octocameratus (Cushman and 118ft (latest Eocene or earliest Oligocene).—The for Hanna), Bolivina, Lagena, Textularia, Pyramidina, Trifa- aminifers in the sample from 118 ft are moderately to highly rina, and Uvigerina. A moderate number of planktonic recrystallized. Cibicides is the most abundant benthic taxon, specimens are present, including Pseudohastigerina micra and lesser numbers of Siphonina, Gyroidinoides, and (Cole) and Cheiloguembelina. The foraminiferal assem Eponides are present. A small proportion of adult plank blage suggests water depths of 100 to 200 ft. This assem tonic foraminifers is present. No age-diagnostic taxa were blage is similar to those found in the two overlying samples noted. The assemblage suggests shallow-marine environ of the Santee Limestone. These assemblages suggest ments, probably in the deeper portion of the 0- to 100-ft slightly deeper water environments than those found in the depth interval. underlying sample from the upper part of the Warley Hill Formation. 355 ft (late middle Eocene).—The foraminifers in the MILLERS POND CORE sample from 355 ft are slightly to moderately recrystallized. A diverse benthic assemblage similar to that of the underly The continuously cored Millers Pond test hole (GGS- ing sample is present, along with a small to moderate pro 3758, Burke 2) in Burke County, Ga. (fig. 1), penetrated portion of planktonic specimens. Cibicides westi Howe, Upper Cretaceous through upper Eocene deposits. The land Pseudononion, Siphonina claibornensis Cushman, Gyroidi surface elevation is 245 ft at the drill site. The site is located noides octocameratus (Cushman and Hanna), Pyramidina, at lat 33°13'48" N., long 81°52'44" W. This test hole is in a and Lagena, are present among other benthic taxa. The more upbasin location than is the Millhaven test hole, and assemblage suggests water depths of 100 to 200 ft. beds containing calcareous microfossils are much less 346 ft (late middle Eocene).—The foraminifers in the numerous. Only three Cenozoic samples, between a depth sample from 346 ft range from moderately well preserved to of 148 and 82 ft, yielded foraminifers (table 2, fig. 3). Fora slightly recrystallized. A diverse benthic assemblage minifers in all three assemblages are moderately to highly includes Pseudononion, Cibicides westi Howe, Gyroidi recrystallized. The three samples are from strata placed in noides octocameratus (Cushman and Hanna), Siphonina the Santee Limestone of middle Eocene age (Falls and claibornensis Cushman, Valvulineria, Nonionella, Anomali- Prowell, this volume, chap. A). The uppermost sample at noides, Hanzawaia, Bolivina, Pararotalia, Trifarina, Textu- 82-83 ft is in carbonate-rich quartzose sand of the upper laria, Spiroplectammina, Guembelitria columbiana Howe, Three Runs Aquifer of Clarke and others (1994). The under and Lagena. A small proportion of planktonic specimens is lying samples from 148 ft and 120 ft are in carbonate-rich FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 111

~~Table 2. Sedimentary characteristics of foraminiferal samples from the Millers Pond core.~~

~~Sample depth (ft) Sedimentary characteristics~~

~~Santee Limestone~~

82-83—————— Carbonate-rich quartzose sand; 59 percent sand size by weight; quartz composes 75 percent of the sand-sized mate rial with carbonate as the remainder; quartz is very angular to angular; echinoid spines present; no glauconite present, but there are trace amounts of red jasper and obsidian. 120——————— Carbonate sand; 77 percent sand size by weight, and all is carbonate; echinoid spines present; no glauconite present.

148——————— Calcareous silty sand; 93 percent sand size by weight; sand fraction mostly carbonate with only 5 percent angular to subangular quartz; no glauconite present, but there are trace amounts of obsidian and chalcopyrite.

and quartz-poor sediments of the lower confining unit of ocassidulina, Gyroidina, and Cibicides westi Howe. this aquifer system. The general lithologic nature of each Pseudohastigerina micra (Cole) is the only planktonic spe sample and the most important foraminiferal components of cies noted. Cibicides westi Howe is characteristic of middle each sample are given below. More detailed sedimentologic Eocene strata in the Southeastern United States, being found information is in table 2. in the Lisbon and Gosport Formations in Alabama (Bandy, 1949), other middle Eocene strata in Georgia (Herrick, 1961), and middle Eocene strata in North Carolina (Jones, SANTEE LIMESTONE 1983). The presence of this species suggests a middle Eocene age for this sample. Most foraminifers from the Santee Limestone in the The generic composition of the benthic foraminiferal Millers Pond core are moderately to highly recrystallized. assemblage and the presence of only a few planktonic spec The identifiable taxa suggest shallow-marine environments imens suggests shallow-marine, probably well-oxygenated with water depths of 100 ft or shallower for the calcareous depositional environments having water depths less than sediments of the three samples from the Santee Limestone. 100 ft. The faunal similarity to Alabama middle Eocene fau There is considerable variability in the proportion of quartz nas and the carbonate substrate suggest warm temperate to grains in these sands. subtropical paleotemperatures. The abundance of Cibicides 148ft (middle Eocene).—The sample from 148 ft is a and Hanzawaia specimens and the presence of echinoid calcareous, slightly silty sand that contains a small amount spines in the sample suggest a relatively firm substrate dur (5 percent) of quartz. Few foraminifers are present, and ing deposition. The absence of glauconite in the sample may most of these are poorly preserved. The specimens mainly suggest moderately high sedimentation rates, as the appar belong to several species of Cibicides (but C. westi Howe is ently open marine conditions would not preclude glauconite not present) with a few poorly preserved miliolid specimens formation, which was common in this time interval in other probably belonging to Quinqueloculina. No species known areas in the Southeastern United States. to be significant biostratigraphically were recognized in the 82-83 ft (middle Eocene).—The sample from 82-83 ft assemblage. is a carbonate-rich quartzose sand. The benthic assemblage Because of the poor state of preservation and the likely is moderately to highly recrystallized, which makes it diffi removal of some or many species of the original foramin cult to identify specimens to the species level. The benthic iferal assemblage, little definitive interpretation of the pale- assemblage is dominated by taxa of Discorbis, Hanzawaia, oenvironments is possible. The species found in the sample Elphidium, Nonion, Cibicides, Cancris, and Textularia. The are in keeping with a warm marine environment with water sample contains common specimens of Cibicides westi depths of less than 100 ft as found for the overlying two Howe, which is characteristic of middle Eocene strata, and samples discussed below. Cancris involutus Copeland, which is found in middle 120 ft (middle Eocene).—The sample from 120 ft is a Eocene beds in North Carolina (Jones, 1983). No planktonic carbonate sand that does not contain quartz grains. Foramin specimens were noted. iferal specimen preservation ranges from moderately to The generic composition of the foraminiferal assem highly recrystallized. This assemblage contains more genera blage suggests a shallow-marine, probably well-oxygenated than noted in the overlying sample at 82-83 ft, but this depositional environment having water depths less than 100 higher diversity may reflect only the better preservation that ft, similar to that proposed for the underlying sample. A sig is present in this sample. The dominant benthic forms nificant quartzose sand component is present in this sample belong to Hanzawaia and Cibicides, but the sample also in contrast with its absence in the underlying two samples. contains Nonion, Elphidium, Bolivina, Lenticulina, Glob- Its presence suggests possible shallowing of the marine 112 GEOLOGY AND PALEONTOLOGY OF FIVE CORES FROM SCREVEN AND BURKE COUNTIES, GEORGIA environment or a change in the sediment source, transporta core. This paleobathymetric interpretation suggests that the tion system, or energy level in the depositional regime of upbasin-downbasin relationship now present in these two this interval. cores is similar to that present during the middle Eocene. Depositional environments generally had near-normal to normal oxygenation levels except for an interval in early CONCLUSIONS late Paleocene time. This interval is represented by beds of the Ellenton Formation where high-nutrient and (or) Foraminiferal assemblages indicative of late early and low-oxygen environments were present as reflected by the early late Paleocene and middle Eocene ages are present in benthic foraminiferal assemblage. The sediments in this the more downbasin Millhaven test hole. A late early Pale interval, however, are bioturbated and contain some small ocene age assignment for the lowest beds of the Ellenton clam shells, so oxidation levels were not so low as to pre Formation is based on the co-occurrence of planktonic fora- clude some bottom organic activity. miniferal taxa and calcareous nannofossil taxa. Early late Paleocene and middle Eocene age assignments are based on the ranges of benthic foraminiferal taxa in the Southeastern REFERENCES CITED United States. More detailed age assignments of the strata on the basis of the foraminifers are not possible. This is Bandy, O.L., 1949, Eocene and Oligocene Foraminifera from Lit because the ranges of most benthic taxa in terms of the tle Stave Creek, Clarke County, Alabama: Bulletins of Ameri intercontinental zonations, which are largely based upon can Paleontology, v. 32, 210 p. planktonic microfossils, are not yet known, and diagnostic Berggren, W.A., Kent, D.V., Swisher, C.C., III, and Aubry, M.-P., planktonic foraminiferal species are not present in most 1995, A revised Cenozoic geochronology and chronosrratig- beds. Detailed age assignments of most foraminifer-bearing raphy, in Berggren, W.A., Kent, D.V., Aubry, M.-P, and Hard- beds were possible, however, on the basis of the calcareous enbol, Jan, eds., Geochronology, time scales and global stratigraphic correlation: SEPM (Society for Sedimentary nannofossils (Bybell, this volume, chap. F). Geology) Special Publication 54, p. 129-212. In the Millhaven core, one sample from the Ellenton Bybell, L.M., and Gibson, T.G., 1991, Calcareous nannofossils and Formation contains both early Paleocene planktonic fora foraminifers from Paleocene and Eocene strata in Maryland miniferal specimens and calcareous nannofossils diagnostic and Virginia, in Gibson, T.G., and Bybell, L.M., leaders, Pale- of the lower part of the upper Paleocene. The planktonic for ocene-Eocene boundary sedimentation in the Potomac River aminifers apparently were derived during erosional removal Valley, Virginia and Maryland: I.G.C.P (International Geo of lower Paleocene strata in this area and reworked into the logical Correlation Programme) Project 308 Field Trip Guide basal part of the lower upper Paleocene transgressive book, p. 15-29. sequence. Lower Paleocene strata that are now eroded from Clarke, J.S., Falls, W.F., Edwards, L.E., Frederiksen, N.O., Bybell, this area apparently represent middle to outer neritic envi L.M., Gibson, T.G., and Litwin, R.J., 1994 [1995], Geologic, ronments because the reworked assemblages are dominated hydrologic and water-quality data for a multi-aquifer system by planktonic specimens. Similar situations of abundant in coastal plain sediments near Millers Pond, Burke County, Georgia, 1992—93: Georgia Geologic Survey Information Cir deeper water lower Paleocene specimens being reworked cular 96, 34 p., 1 pi. in pocket. into shallow-water lower upper Paleocene beds are also Copeland, C.W., 1964, Eocene and Miocene Foraminifera from present in Atlantic Coastal Plain deposits in North Carolina two localities in Duplin County, North Carolina: Bulletins of and Virginia. American Paleontology, v. 47, p. 209-324. In the more upbasin Millers Pond core, foraminiferal Gibson, T.G., 1988, Assemblage characteristics of modern benthic assemblages were obtained only from the Santee Lime Foraminifera and application to environmental interpretation stone. The assemblages contain benthic species characteris of Cenozoic deposits of eastern North America: Revue de tic of a middle Eocene age. Paleobiologie, special issue 2, p. 777-787. Most foraminifer-bearing beds examined in the two ————1989, Planktonic benthonic foraminiferal ratios—Modern cores were deposited in inner neritic (0- to 100-ft water patterns and Tertiary applicability: Marine Micropaleontol- depth) to inner-middle neritic (100- to 200-ft water depth) ogy, v. 15, p. 29-52. environments. One interval in the Congaree Formation, in -1992, Lithologic changes in fluvial to marine depositional the early middle Eocene, at 481.5 ft, contains assemblages systems in Paleogene strata of Georgia and Alabama, in Gohn, G.S., ed., Proceedings of the 1988 U.S. Geological suggestive of deeper water environments with depths Survey Workshop on the Geology and Geohydrology of the around 300 ft. Some intervals in the upper middle Eocene Atlantic Coastal Plain: U.S. Geological Survey Circular 1059, strata of the Santee Limestone in the more southeasterly, p. 109-113. more downbasin Millhaven core suggest slightly deeper Gibson, T.G., Andrews, G.W., Bybell, L.M., Frederiksen, N.O., water environments (inner-middle neritic) than presumably Hansen, Thor, Hazel, I.E., McLean, D.M., Witmer, R.J., and coeval inner neritic strata of the Santee Limestone, which is Van Nieuwenhuise, D.S., 1980, Biostratigraphy of the Ter found in the more northwesterly, more upbasin Millers Pond tiary strata of the core, in Geology of the Oak Grove core: FORAMINIFERA FROM THE MILLHAVEN AND MILLERS POND CORES, GEORGIA 113

Virginia Division of Mineral Resources Publication 20, pt. 2, Herrick, S.M., 1961, Well logs of the coastal plain of Georgia: p. 14-30. Georgia Geologic Survey Bulletin 70, 462 p. Gibson, T.G., and Buzas, M.A., 1973, Species diversity: patterns in Jones, G.D., 1983, Foraminiferal biostratigraphy and depositional modern and Miocene Foraminifera of the eastern margin of history of the middle Eocene rocks of the coastal plain of North America: Geological Society of America Bulletin, v. North Carolina: North Carolina Geological Survey Section 84, p. 217-238. Special Publication 8, 80 p., 16 pis. Gibson, T.G., and Bybell, L.M., 1994, Paleogene stratigraphy of Martini, Erlend, 1971, Standard Tertiary and Quaternary calcare the Solomons Island, Maryland corehole: U.S. Geological Survey Open-File Report 94-708, 39 p. ous nannoplankton zonation: Planktonic Conference, 2d, Rome, 1969, Proceedings, p. 739-785. ————1995, Sedimentary patterns across the Paleocene-Eocene boundary in the Atlantic and Gulf Coastal Plains of the Murray, J.W., 1991, Ecology and palaeoecology of benthic Fora United States: Societe Beige de Geologic Bulletin, v. 103, p. minifera: New York, John Wiley & Sons, 397 p. 237-265. Nogan, D.S., 1964, Foraminifera, stratigraphy, and paleoecology Gibson, T.G., Bybell, L.M., and Govoni, D.L., 1991, Paleocene of the Aquia Formation of Maryland and Virginia: Cushman and Eocene strata of the central Atlantic Coastal Plain, in Foundation for Foraminiferal Research Special Publication 7, Gibson, T.G., and Bybell, L.M., leaders, Paleocene-Eocene 50 p. boundary sedimentation in the Potomac River Valley, Virginia Olsson, R.K., and Wise, S.W., Jr., 1987, Upper Paleocene to mid and Maryland: I.G.C.P. (International Geological Correlation dle Eocene depositional sequences and hiatuses in the New Programme) Project 308 Field Trip Guidebook, p. 1-13. Jersey Atlantic margin: Cushman Foundation for Foramin Gibson, T.G., Bybell, L.M., and Owens, J.P., 1993, Latest Pale iferal Research Special Publication 24, p. 99-112. ocene lithologic and biotic events in neritic deposits of south western New Jersey: Paleoceanography, v. 8, p. 495-514. Poag, C.W., 1989, Foraminiferal stratigraphy and paleoenviron- Gohn, G.S., 1988, Late Mesozoic and early Cenozoic geology of ments of Cenozoic strata cored near Haynesville, Virginia, the Atlantic Coastal Plain: North Carolina to Florida, in chap. D o/Mixon, R.B., ed., Geology and paleontology of the Sheridan, R.E., and Grow, J.A., eds., The Atlantic continental Haynesville cores—Northeastern Virginia Coastal Plain: U.S. margin; U.S., v. 1-2 o/The geology of North America: Boul Geological Survey Professional Paper 1489, 20 p, 5 pis. der, Colo., Geological Society of America, p. 107-130. Toumarkine, Monique, and Luterbacher, Hanspeter, 1985, Pale Haq, B.U., Hardenbol, Jan, and Vail, PR., 1987, Chronology of ocene and Eocene Foraminifera, in Bolli, H.M., Saunders, fluctuating sea levels since the Triassic: Science, v. 235, p. J.B., and Perch-Nielsen, Katharina, eds., Plankton stratigra 1156-1167. phy: New York, Cambridge University Press, p. 87-154.

~~PLATE 1 PLATE 1~~

[Illustrated specimens are from the indicated depths in the Millhaven core, Screven County, Georgia. All specimens are benthic except for Globoconusa daitbjergensis. USNM, U.S. National Museum of Natural History, Washington, D.C.]

Figure 1. Nodogenerina plummerae (Cushman), USNM 493350 (628.7 ft), Ellenton Formation, side view (x 85). 2. Pseudanodosaria tenuistriata (Franke), USNM 493351 (628.7 ft), Ellenton Formation, side view (x 42). 3. Globoconusa daubjergensis (Bronnimann), USNM 493352 (631.3 ft), Ellenton Formation, spiral view (x 292). 4. Globoconusa daubjergensis (Bronnimann), USNM 493353 (631.3 ft), Ellenton Formation, side view (x 256). 5. Pyramidina virginiana (Cushman), USNM 493354 (593.7 ft), Ellenton Formation, side view (x 228). 6. Pulsiphonina prima (Plummer), USNM 493355 (631.3 ft), Ellenton Formation, spiral view (x 148). 7. Pulsiphonina prima (Plummer), USNM 493356 (628.7 ft), Ellenton Formation, umbilical view (x 182). 8. Siphonina daibornensis Cushman, USNM 493357 (355 ft), Santee Limestone, umbilical view (x 104). 9. Cibicides compressus Olsson, USNM 493358 (631.3 ft), Ellenton Formation, spiral view (x 148). 10, 11. Cibicides compressus Olsson, USNM 493359 (631.3 ft), Ellenton Formation; 10, side view (x 149); 11, umbilical view (x 148). 12. Cibicides neelyi Jennings, USNM 493360 (631.3 ft), Ellenton Formation, umbilical view (x 91). 13. Pararotaliaperclara (Loeblich and Tappan), USNM 493361 (628.7 ft), Ellenton Formation, spiral view (x 287). 14. Pararotalia perclara (Loeblich and Tappan), USNM 493362 (628.7 ft), Ellenton Formation, umbilical view (x 297). 15, 16. Cibicides westi Howe, USNM 493363 (355 ft), Santee Limestone; 15, umbilical view (x 170); 16, side view (x 174). U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1603-1, PLATE 1

~~NODOGENERINA, PSEUDONODOSARIA, GLOBOCONUSA, PYRAMIDINA, PULSIPHONINA, SIPHONINA, CIBICIDES, AND PARAROTALIA~~

* U.S. GOVERNMENT PRINTING OFFICE: 2001 — 673-049 / 30019 Region No. 8

~~Selected Series of U.S. Geological Survey Publications~~

Books and Other Publications Miscellaneous Investigations Series Maps or Geologic Investigations Series (I's) are on planimetric or topographic Professional Papers report scientific data and interpretations bases at various scales; they present a wide variety of format of lasting scientific interest that cover all facets of USGS inves and subject matter. The series also incudes 7.5-minute quadran tigations and research. gle photogeologic maps on planimetric bases and planetary maps. Bulletins contain significant data and interpretations that are of lasting scientific interest but are generally more limited in Information Periodicals scope or geographic coverage than Professional Papers. Metal Industry Indicators (Mil's) is a free monthly newslet Water-Supply Papers are comprehensive reports that present ter that analyzes and forecasts the economic health of five significant interpretive results of hydrologic investigations of metal industries with composite leading and coincident wide interest to professional geologists, hydrologists, and engi indexes: primary metals, steel, copper, primary and secondary neers. The series covers investigations in all phases of hydrol aluminum, and aluminum mill products. ogy, including hydrogeology, availability of water, quality of water, and use of water. Mineral Industry Surveys (MIS's) are free periodic statistical and economic reports designed to provide timely statistical data Circulars are reports of programmatic or scientific information on production, distribution, stocks, and consumption of signifi of an ephemeral nature; many present important scientific cant mineral commodities. The surveys are issued monthly, information of wide popular interest. Circulars are distributed quarterly, annually, or at other regular intervals, depending on at no cost to the public. the need for current data. The MIS's are published by commod Fact Sheets communicate a wide variety of timely information ity as well as by State. A series of international MIS's is also on USGS programs, projects, and research. They commonly available. address issues of public interest. Fact Sheets generally are two Published on an annual basis. Mineral Commodity Summa or four pages long and are distributed at no cost to the public. ries is the earliest Government publication to furnish estimates covering nonfuel mineral industry data. Data sheets contain Reports in the Digital Data Series (DDS) distribute large information on the domestic industry structure, Government amounts of data through digital media, including compact disc- programs, tariffs, and 5-year salient statistics for more than 90 read-only memory (CD-ROM). They are high-quality, interpre individual minerals and materials. tive publications designed as self-contained packages for view ing and interpreting data and typically contain data sets, The Minerals Yearbook discusses the performance of the software to view the data, and explanatory text. worldwide minerals and materials industry during a calendar year, and it provides background information to assist in inter Water-Resources Investigations Reports are papers of an preting that performance. The Minerals Yearbook consists of interpretive nature made available to the public outside the for three volumes. Volume I, Metals and Minerals, contains chap mal USGS publications series. Copies are produced on request ters about virtually all metallic and industrial mineral commod (unlike formal USGS publications) and are also available for ities important to the U.S. economy. Volume II, Area Reports: public inspection at depositories indicated in USGS catalogs. Domestic, contains a chapter on the minerals industry of each Open-File Reports can consist of basic data, preliminary of the 50 States and Puerto Rico and the Administered Islands. reports, and a wide range of scientific documents on USGS Volume III, Area Reports: International, is published as four investigations. Open-File Reports are designed for fast release separate reports. These reports collectively contain the latest and are available for public consultation at depositories. available mineral data on more than 190 foreign countries and discuss the importance of minerals to the economies of these nations and the United States. Maps Permanent Catalogs Geologic Quadrangle Maps (GQ's) are multicolor geologic maps on topographic bases in 7.5- or 15-minute quadrangle "Publications of the U.S. Geological Survey, 1879-1961" formats (scales mainly 1:24,000 or 1:62,500) showing bedrock, and "Publications of the U.S. Geological Survey, 1962- surficial, or engineering geology. Maps generally include brief 1970" are available in paperback book form and as a set of texts; some maps include structure and columnar sections only. microfiche.

Geophysical Investigations Maps (GP's) are on topographic "Publications of the U.S. Geological Survey, 1971-1981" is or planimetric bases at various scales. They show results of available in paperback book form (two volumes, publications geophysical investigations using gravity, magnetic, seismic, or listing and index) and as a set of microfiche. radioactivity surveys, which provide data on subsurface struc Annual supplements for 1982, 1983, 1984, 1985, 1986, and tures that are of economic or geologic significance. subsequent years are available in paperback book form.